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ORIGINAL ARTICLE
Stromatolites in the Paratethys Sea during the Middle Mioceneclimate transition as witness of the Badenian salinity crisis
Mathias Harzhauser • Jorn Peckmann •
Daniel Birgel • Erich Draganits • Oleg Mandic •
Dorte Theobalt • Julian Huemer
Received: 6 October 2013 / Accepted: 28 November 2013 / Published online: 12 December 2013
� Springer-Verlag Berlin Heidelberg 2013
Abstract This is the first documentation of Middle
Miocene (late Langhian) stromatolites from the Central
Paratethys Sea. These microbialites formed in a lagoonal
setting in the Austrian Oberpullendorf Basin, which is part
of the Pannonian Basin Complex. Sedimentological and
paleontological data indicate that an initial marine trans-
gression led to the establishment of a gravelly and sandy
shore. Subsequently, an agitated lagoon with shallow-
marine sublittoral conditions and a diverse mollusc fauna
developed. Diminishing accommodation space forced the
development of a restricted, muddy lagoon. A rather hostile
environment and probably hypersaline conditions led to the
disappearance of metazoans and triggered the formation of
a short succession of microbialites. Minor oscillations of
the relative sea-level are reflected by alternations of
undulate/planar stromatolites to domal stromatolites and
distorted stromatolites with frequent emersion surfaces.
The microbialites can be traced across a large area of the
basin. They are coeval with the thick evaporites of the
Carpathian Foredeep and the Transylvanian Basin, which
formed during the Badenian salinity crisis. This coinci-
dence suggests that the mid-Badenian Paratethyan stro-
matolites are ecological analogs of Mediterranean
stromatolites that formed during the Messinian salinity
crisis.
Keywords Microbialites � Molluscs � Miocene �Badenian � Paratethys Sea � Badenian salinity crisis
Introduction
Microbial sediments are very specific indicators of envi-
ronmental conditions (Riding and Awramik 2000). In this
respect, Miocene stromatolites of the Mediterranean
basins have received increasing attention by the scientific
community in the context of the Messinian salinity crisis
(Riding et al. 1991; Martın et al. 1993; Martın and Braga
1994; Braga et al. 1995; Calvet et al. 1996; Esteban 1996;
Feldmann and McKenzie 1997; Braga and Martın 2000;
Oliveri et al. 2010; Arenas and Pomar 2010). In contrast,
microbial carbonates of the neighboring Paratethys Sea
are comparatively poorly known so far. The complex
geodynamic and oceanographic history of this epiconti-
nental Eurasian sea is reflected by rapid shifts in its biota
and by numerous severe extirpation events (Harzhauser
M. Harzhauser (&) � O. Mandic � D. Theobalt
Geological-Paleontological Department, Natural History
Museum Vienna, Burgring 7, 1010 Vienna, Austria
e-mail: mathias.harzhauser@nhm-wien.ac.at
O. Mandic
e-mail: oleg.mandic@nhm-wien.ac.at
D. Theobalt
e-mail: doerte.theobalt@nhm-wien.ac.at
J. Peckmann � D. Birgel � E. Draganits � J. Huemer
Department of Geodynamics and Sedimentology,
University of Vienna, Althanstrasse 14,
1090 Vienna, Austria
e-mail: joern.peckmann@univie.ac.at
D. Birgel
e-mail: daniel.birgel@univie.ac.at
E. Draganits
e-mail: erich.draganits@univie.ac.at
J. Huemer
e-mail: julian_huemer@sbg.at
E. Draganits
Department of Prehistoric and Historical Archaeology,
University of Vienna, Franz-Klein-Gasse 1,
1190 Vienna, Austria
123
Facies (2014) 60:429–444
DOI 10.1007/s10347-013-0391-z
and Piller 2007). The seesaw changes between normal-
marine and strongly restricted conditions are also
expressed by varied lithologies including black shales,
diatomites, halites, sulfates, iron ooids, and various mi-
crobialites (Popov et al. 2004; Schulz et al. 2005; Piller
et al. 2007; Vasiliev et al. 2011; Peryt 2013). In the Pa-
ratethys Sea, microbialites had a heyday during the Late
Serravallian (Sarmatian) when restricted marine connec-
tions and strongly aberrant water chemistry boosted the
establishment of these carbonate deposits, which were
usually associated with bryozoans and serpulids in build-
ups (Piller and Harzhauser 2005; Daoud et al. 2006;
Cornee et al. 2009). Similar microbial-serpulid build-ups
formed even earlier during the Middle Miocene in the
Eastern Paratethys during phases of restricted water
exchange (Peryt et al. 2004). No similar carbonate build-
ups, however, are known so far from the Central Parate-
thys, where normal-marine conditions prevailed. Only
coral reef-associated microbial crusts were documented
from this area by Saint-Martin et al. (2000). Carbonate
microbialites, e.g., stromatolites and thrombolites (sensu
Shapiro 2000; Riding 2011), not supported by a frame-
work of metazoans are unknown from the Paratethys Sea
so far, although stromatolitic gypsum developed in the
Carpathian Foredeep (Peryt 2013). Therefore, the herein-
documented occurrence of Middle Miocene (Badenian)
stromatolites from the Austrian Oberpullendorf Basin is
an exceptional opportunity to contribute to the under-
standing of Paratethyan ecosystems.
Geological setting
The investigated sections expose gravel, sand, marls, and
limestones of the Ritzing Formation, which comprises
shallow-marine Middle Miocene deposits of the Oberpul-
lendorf Basin (Zorn 2000). This small basin is limited by
Lower Miocene fluvial gravel in the north, by Lower
Austro-Alpine metamorphic units of the so-called Bucklige
Welt in the west, and by the Penninic units of the Guns
Mountains in the south (Draganits 1998; Zorn 2000)
(Fig. 1). Towards the east, it is connected to the huge
Pannonian Basin Complex. Tectonically, the investigated
sections are located at the boundary between the Eastern
Alps and the Hungarian Basin with tectonic activity start-
ing before the Miocene and still being active today (Dra-
ganits 1996; Szekely et al. 2009). As a consequence,
sedimentation in this area was strongly influenced by the
pre-existing topography resulting from crustal thickening
during the Alpine Orogeny and syn-sedimentary vertical
crustal movements. Additionally, post-depositional tec-
tonic movements result in the juxtaposition of sediments of
identical age and depositional environment at different
altitudes. The main orientation of brittle faults trend
northwest–southeast and east–west (Draganits 1996) and
extension resulted in Horst-Graben type of deformation,
which is well documented in the coal mines of Bren-
ngbergbanya and Ritzing, where fault throws up to 180 m
have been recorded (Vendl 1933; Kishazi and Ivancsics
1977).
Fig. 1 Geographic setting of the Oberpullendorf Basin close to the Austrian/Hungarian border (left) and position of the investigated sections
(right; satellite image taken from Google Earth); Ra CY, community building-yard
430 Facies (2014) 60:429–444
123
The two investigated sections (Ritzing 1 and Rabenk-
ropf) are positioned at the northern margin of the Ober-
pullendorf Basin, which was a small embayment at the
north-western coast of the Paratethys Sea [see Rogl (1998)
and Popov et al. (2004) for detailed reviews on the Parat-
ethys Sea and Piller et al. (2007) for correlation of the
regional stages]. Marine deposition started during the
Badenian (=Langhian and early Serravallian) and ended
during the late Sarmatian (=late Serravallian). Detailed
mapping of the area by Janoschek (1931) and Mostafavi
(1978) revealed the occurrence of three depositional cycles
during the Badenian. The first ingression is reflected by the
deposition of mollusc-rich marls, calcareous sand, and
corallinacean limestones. The benthic foraminifers of this
unit allow a correlation with the regional Upper Lagenidae
Zone of Grill (1943) and the occurrence of Orbulina sut-
uralis points to the planktonic foraminiferal zone M6 of
Berggren et al. (1995). The next depositional cycle is also
characterized by shallow-marine conditions. Fossil-rich
sand accumulated during this phase in coastal settings and
thick corallinacean limestones developed in the sublittoral
areas. The foraminifers are characteristic of the regional
Spirorutilus Zone (Sieber 1956; Mostafavi 1978) coincid-
ing largely with the middle part of the Badenian stage. The
stromatolites of the Rabenkropf section are located at the
top of this second depositional cycle. A third succession,
corresponding to the late Badenian (=early Serravallian) is
recorded by scattered patches of clay and sand suggesting
that only southern parts of the basin became reflooded
(Mostafavi 1978). The widespread Sarmatian and Panno-
nian sediments towards the center of the Oberpullendorf
Basin are not the scope of this study.
Ritzing 1 section (Ri 1: N47�3705.4800 E16�3005.2100,370 m a.s.l.)
The stratigraphically lowermost beds crop out in the Rit-
zing 1 section, located 140 m NNW of the Rabenkropf
Section in a deeply incised gully. There, an about 7-m-
thick succession of partly cross-bedded, poorly sorted sand
and channels with coarse gravel and pebbles, is exposed in
a steep cliff. Despite the overall fluvial appearance of the
sediments, the occurrence of clionid sponge borings in the
gravels and scattered pebbles with attached and articulated
specimens of the oyster Ostrea digitalina (Dubois, 1831)
clearly indicate a marine depositional environment. The
pebbles probably represent reworked Lower Miocene
(Ottnangian = middle Burdigalian) fluvial gravel of the
Auwald Gravel Formation, which is widespread in the
Oberpullendorf Basin (Janoschek 1931; Zorn 2000). Rit-
zing 1 beds dip gently towards the south-southeast (Rup-
precht 2011). No major faults are visible between the
investigated outcrops. However, the occurrence of
abundant deformation bands in the sediments of this sec-
tion (Rupprecht 2011) may indicate the presence of nearby
faults, obscured by the dense vegetation. Taking into
account bed-dipping values and the topographic positions
of both outcrops, the thickness of unexposed sediments
between both sections is estimated to be only some meters.
Rabenkropf section (RaS: N47�3700.15500
E16�30008.5300; 383 m a.s.l.; Figs. 2, 3)
The RaS is located close to the top of a small hill ENE of
Ritzing in Burgenland/Austria. Beds dip 10�–20� towards
SSW. The section is part of an abandoned quarry, which is
nearly completely covered by vegetation and scree at pres-
ent. Therefore, only the uppermost 3 m (=RaS) could be
investigated in detail. The succession underneath ([12 m),
between RaS and the community building-yard (referred to
as Ra CY), is mostly inaccessible. Single carbonate beds,
outcropping along the slope close to the community build-
ing-yard at 370 m a.s.l., revealed the presence of bioclastic,
peloidal packstones to grainstones with numerous ostracods,
foraminifers, and molluscs along with oyster floatstones
containing Ostrea digitalina in the basal part of the succes-
sion. There, bindstones incorporating masses of hydrobiid
gastropods and specimens of the mud creeper Granulolabi-
um bicinctum (Brocchi, 1814) (Fig. 4a) have been recorded.
In thin-section, the bindstones lack stromatolitic fabrics but
consist of fine-grained laminated peloidal packstones with
thin peloidal grainstone interlayers (Fig. 4b).
Ra 1–3 (113 cm; base covered; Figs. 5, 6)
The exposed part of the succession forms a cliff of about
4-m width and a total height of 3.6 m (Figs. 2, 3). The
section starts with yellow-orange, friable, bioclastic cortoid
pack-/grainstones with dense mollusc coquinas (Fig. 5a),
partly forming mollusc rudstones. Aragonitic shells have
been completely dissolved, but the remaining cavities
allow a clear identification of the species based on silicone
molds (Fig. 5b). The lower 60 cm of this unit (Ra 1)
contains moderately dense coquinas consisting mainly of
turritellid gastropods and cardiid bivalves. A serpulid-
bivalve bioherm of *30 cm in diameter and 20 cm in
thickness occurs in Ra 2A (Fig. 6). The dominant bivalves
in the bioherm are modiolids along with some oysters. The
modiolids form a dense in situ colony in the center of the
bioherm and are still articulated (Fig. 6a); they are over-
grown by a dense colony of serpulid tubes, which are
tentatively identified as Hydroides (Fig. 6b). Large cavities
within the bivalves display geopetal sediment structures.
The density of the coquinas increases within the following
55 cm (Ra 2B–C). Turritellids, cardiids, and oysters pre-
dominate; the bivalves are disarticulated and the
Facies (2014) 60:429–444 431
123
Fig. 2 The Rabenkropf section
with characteristic
paleontological and lithological
features based on logging in
2013 (sample numbers
correspond to bed numbers)
432 Facies (2014) 60:429–444
123
orientation of the shells is random. The most abundant
species are: Acanthocardia turonica (Hornes, 1861), Tur-
ritella erronea Cossmann in Friedberg, 1914, Ostrea dig-
italina (Dubois, 1831), Corbula gibba (Olivi, 1792), and
Venus nux (Gmelin, 1791) accompanied by Thericium eu-
ropaeum (Mayer, 1878), Nassarius schoenni (Hoernes &
Auinger, 1882), Neverita olla (de Serres, 1829), Aporrhais
alata (Eichwald, 1830), Terebralia duboisi (Hornes, 1855),
Granulolabium bicinctum (Brocchi, 1814), and Xenophora
deshayesi (Michelotti, 1847). Only Panopea menardi
Deshayes, 1829, occurs in situ with articulated bivalves,
forming a moderately dense gallery of specimens. The
uppermost 10 cm of bed Ra 2C is intensively colored by
reddish-brown speckles and is partly altered into caliche.
The transition into the overlying stromatolitic unit is
marked by 7 cm of olive-grey, laminated silty marl (Ra 3).
The foraminiferal assemblage of this marl consists of Po-
rosononion granosum (d’Orbigny, 1826), Nonion commune
(d’Orbigny, 1826), Elphidium fichtelianum (d’Orbigny,
1846), and Ammonia beccarii (Linnaeus, 1758).
The stromatolites form a more than 1.4-m-thick suc-
cession, which comprises several discrete stromatolite sub-
beds (Ra 4A–Ra 4H) exhibiting different macroscopic
growth forms. Secondary manganese and iron-oxide den-
drites and coatings are characteristic in all thin-sections.
Ra 4A (8 cm; Fig. 7)
The laminated, planar-bedded unit with continuous laminae
is overlain by 2 cm of gray marl. Ra 4A starts with a sharp
boundary and a 1-cm-thick yellow ostracod packstone
containing partly articulated ostracods. A distinctly lami-
nated bindstone is sharply developed above the basal
packstone (Figs. 7a). Flat micritic dark laminae predomi-
nate. They have a thickness of *1 to 1.8 mm and are
separated by subordinate light laminae of *0.1 to 0.5 mm
thickness and larger laminoid fenestrae. Towards the top,
the dark laminae become wrinkled, and are separated into
single, smaller laminae (*0.05 to 0.1 mm) alternating with
closely spaced thin microsparitic laminae of similar
thickness (Fig. 7b). The laminoid fenestrae are replaced by
large isolated vugs. Some of the cavities can be attributed
to serpulids that grew parallel to the bedding surface on the
microbial mats (Fig. 7c).
Ra 4B (*18 cm; Fig. 8)
The well-laminated, planar-bedded stromatolite with in-
terlayers of crinkled laminae terminates in a 4- to 10-cm-
thick alternation of gray marls and microbialite mats. Mi-
critic intercalations, 1–2 cm in thickness, lacking laminae
Fig. 3 Outcrop picture of the Rabenkropf section (July 2013) and
interpretation of bedding surfaces and stromatolite growth forms;
colors, signatures, and bed numbers correspond to Fig. 2; note the
increase in relief of single stromatolite layers within RA 4A–G; the
white ellipse in Ra 2B indicates an in situ Panopea menardi; hammer
for scale
Facies (2014) 60:429–444 433
123
display angular and polygonal cavities formed by dissolved
chips of microbial mats.
Ra 4C (*8 cm) and 4D (*15 cm; Fig. 9)
Eight laminated sub-beds, 2–5 cm thick, with low, undu-
lating relief. Basal parts of the beds are usually planar
bedded and grade via crinkled laminae into low-relief
colloform stromatolites with large fenestrae and/or very
low relief domal stromatolites. Continuous light laminae,
0.9–1.2 mm thick, predominate in Ra 4C, while intrafor-
mational breccia and discontinuous and amalgamated light
laminae typify Ra 4D.
Ra 4E (*30 cm; Fig. 10)
The unit consists of 3–5 sub-beds of low-domal stro-
matolites up to 5 cm high. Internally, the planar lami-
nation of the basal parts of the sub-beds is
characterized by dense and continuous dark laminae
(*0.5 to 1.5 mm in thickness) alternating with thinner
light laminae with sharp base and irregular tops (*0.1
to 0.4 mm in thickness). The domal to colloform upper
parts of the sub-beds display irregular laminae with
numerous erosional surfaces, strongly reduced dark
laminae and wrinkled, furled, partly discontinuous or
amalgamated light laminae (*0.8 to 1.2 mm); vertical
micro-cracks and strongly wrinkled and contorted
laminae with large vugs are typical. Some light laminae
are strongly fractured and form thin layers of monom-
ict, intraformational breccias with mottled fabric in the
interspaces.
Ra 4F (*15 to 25 cm; Fig. 11c)
Moderately undulate stromatolite passing laterally into
low-colloform stromatolites and dense microbialites,
lacking distinct laminations.
Fig. 4 a Silicone mold of a cross section through a microbialite layer of sample Ra CY close to the community building-yard. 1 Granulolabium
bicinctum, 2 hydrobiid gastropods. b Thin-section of the same sample; hydrobiid gastropods (2) in peloidal pack-/grainstone
434 Facies (2014) 60:429–444
123
Ra 4G (*30 cm; Fig. 11a, b)
Thirty-cm-thick, low-domal to colloform stromatolite. It is
composed of 5–7 sub-beds, which are macroscopically
characterized by coarse wavy lamination and numerous
vugs. In thin-section, rare wavy crinkled laminae alternate
with larger areas of poorly laminated layers and low-col-
loform microbialite layers with clotted fabric; cracks and
large vugs are typical but intraformational breccias are
missing.
The following beds are all strongly weathered and
disintegrated:
Ra 4H (*20 cm; Fig. 12a–c)
The unit consists of 4–5 strongly weathered stromatolite
sub-beds with a wide range of microfacies; well laminated,
planar-bedded areas pass vertically into strongly colloform
distorted parts with high porosity. Laterally intraforma-
tional breccias with nearly completely destroyed primary
fabric occur.
Ra 4I (*90 to 110 cm; Fig. 13a–c)
The high degree of weathering and recent pedogenesis
makes separation of individual layers impossible. The bed
comprises numerous, about 5-cm-thick layers of peloidal
grainstones and stromatolites with largely destroyed pri-
mary fabric. The topmost bed is a 15-cm-thick peloidal
grainstone with mass occurrences of the gastropod Pota-
mides nodosoplicatus (Hornes, 1855) and the bivalve
Diplodonta rotundata (Montagu, 1803) along with rare
oysters and the cerithiid Thericium europaeum (Mayer,
1878).
Fig. 5 a Bioclastic pack/grainstone from Ra 2B; calcitic shells of oysters (1) and pectinids are preserved but aragonitic shells are completely
dissolved (2). b Silicone mold of a coquina of RA 2B, 1 Acanthocardia turonica, 2 Turritella erronea, 3 Terebralia duboisi
Facies (2014) 60:429–444 435
123
Discussion
Paleoecology and depositional environment
Pre-microbialite interval: initial transgression
and formation of an open lagoon
The Ritzing 1 section is situated in the lowest part of the
succession and reflects a marine ingression. Lower Mio-
cene fluvial gravel became reactivated and formed a
gravelly and sandy shore. The highly agitated environment
was colonized only by few specialists such as clionid
sponges, living as borers in the pebbles and oysters (Rut-
zler 1975). The poorly exposed basal parts of the Ra-
benkropf section (Ra CY) document an already completed
switch from siliciclastic towards carbonate sedimentation.
Shallow-marine sublittoral conditions prevailed with mil-
iolid foraminifers, numerous molluscs and ostracods, and
scattered oyster colonies. In the intertidal zone, microbia-
lites developed as indicated by huge populations of grazing
gastropods, such as hydrobiids and Granulolabium bi-
cinctum, which was common in Miocene mudflats (Zus-
chin et al. 2004; d’Amico et al. 2012). The microfacies of
the laminated peloidal pack-/grainstone agrees with a
shallow-marine setting with reduced water circulation
(Flugel 2004).
The mollusc fauna of Ra 1–2 indicates still shallow, but
slightly increased water depths. The predominant Acanth-
ocarida turonica and Turritella erronea along with most
other species point to shallow sublittoral conditions: extant
Acanthocardia species prefer a water depth of 10–15 m
(Rufino et al. 2010); most Turritella species occur in
10–100 m water depth (Allmon 1988) and Corbula gibba
is also most abundant around 10–20 m (Talman and Ke-
ough 2001; Rufino et al. 2010). The presence of nearby
coastal mudflats is reflected by the occurrence of Tere-
bralia, which is restricted to coastal mudflats and man-
groves (Houbrick 1991). The random orientation and
disarticulation of the shells indicates considerable biotur-
bation. The phase of maximum water depth in this lagoon
is documented only indirectly by the presence of in situ
populations of the deep-burrowing Panopea. Modern
geoducks range from the intertidal to about 100-m water
depth and burrow to a depth of 60–120 cm into the sedi-
ment (Alexander and Dietl 2005; Reidy and Cox 2013).
Thus, the position of the shells in a depth of only 20–40 cm
within bed Ra 2 suggests that parts of the overlying sedi-
ment were eroded. Emersion is proven by caliche
Fig. 6 Serpulid-bivalve bioherm from Ra 2A consisting of articulated in situ modiolid bivalves (a) and serpulids most probably representing
Hydroides (b). c Thin-section showing bivalves filled with mudstone and the grainstone matrix between serpulid tubes
436 Facies (2014) 60:429–444
123
Fig. 7 Planar stromatolites (Ra 4A). a Polished slab to show
macroscopic structure. b Thin-section; note the change of lamination
type from thick micritic laminae to disintegrated single laminae in
upwards direction. c Silicone mold of a surface of a stromatolite layer
showing small-scale wrinkles and scattered serpulids on lithified
microbial mats
Fig. 8 Planar stromatolites (Ra 4B): a polished slab to show
macroscopic structure; crinkle lamination alternates with horizontally
laminated layers and micritic layers with angular cavities formed by
dissolved particles, b thin-section showing crinkle lamination in the
base and angular cavities in the upper part; c silicone mold of a
bedding surface reveal the cavities as floating chips of microbial mats
Facies (2014) 60:429–444 437
123
Fig. 9 Low-undulated stromatolites (Ra 4C-D): a polished slab of Ra 4D with dense slightly crinkled and planar lamination; b thin-section of Ra
4C with densely spaced light laminae; c thin-section of Ra 4D with increasing amount of distorted laminae and micro breccia
Fig. 10 Low-relief domical stromatolites (Ra 4E): a weathered
surface displaying contorted laminae and large vugs; thin-sections
showing the transition from continuous laminae towards wrinkled and
partly eroded laminae (b) and largely destroyed primary lamination
with laminae-fragments and mottled fabric (c); note the crack in b,
which originates in layers indicating a phase of erosion
438 Facies (2014) 60:429–444
123
Fig. 11 Low-colloform stromatolites (Ra 4G–F): polished slab a of
Ra 4G revealing distinct stromatolitic laminae alternating with furled
to distorted laminae; b (Ra 4G) and c (Ra 4F) thin-sections showing
poorly laminated layers with strong relief separated by large areas
with clotted fabric
Fig. 12 Stromatolites with intraformational breccias (Ra 4H): polished slab a of a strongly eroded stromatolite lamina chips; b–c: thin-sections
showing the transition from a disrupted stromatolitic fabric (b) into intraformational breccias with destroyed primary structures
Facies (2014) 60:429–444 439
123
formation and pedogenesis in the uppermost parts of Ra 2.
A shallow lagoon, influenced by tidal currents and/or wave
activity, is also in agreement with the predominant bio-
clastic grainstones (Flugel 2004).
Microbialite interval: restricted lagoon
A very shallow, restricted, muddy lagoon with a low
diverse assemblage of non-keeled elphidiid foraminifers
developed during the subsequent re-flooding. Especially
the higher number of Ammonia beccarii hints at a muddy
and hypersaline lagoonal environment (Murray 1991,
2006). Restricted conditions are also indicated by the
individual-rich but low diverse mass occurrence of os-
tracods prior to microbial mat formation.
Morphologically, the following microbialite interval
represents four basic types:
• Laminated, planar bedded stromatolites grading into
laminated marls (Ra 4A, 4B)
• Laminated, low-undulated stromatolites (Ra 4C, 4D)
• Low-relief domal to colloform stromatolites, with
cracks and contorted laminae (Ra 4E, 4F, 4G, 4H)
• Intraformational breccias (Ra 4E, 4H).
Growth of stromatolites is controlled by a set of
extrinsic and intrinsic parameters such as accommodation
space, sedimentation rate, nutrient availability, seawater
chemistry, hydrodynamics, and composition of the micro-
bial community (Feldman and McKenzie 1998; Reid et al.
2000; Riding and Awramik 2000; Andres and Reid 2006;
Seckbach and Oren 2010; Bosak et al. 2013). Potential
modern analogues have been described in great detail from
restricted hypersaline lagoons of Western Australia (Jahn-
ert and Collins 2011, 2012, 2013) and the Gulf of Cali-
fornia (Johnson et al. 2012). Stromatolites and thrombolites
from normal-marine, subtidal settings are documented
from Exuma Cays, Bahamas (Feldman and McKenzie
1998; Andres and Reid 2006). The overall tabular structure
of the Rabenkropf microbialites cannot be compared easily
with the large-scale columnar, domal, and spherical struc-
tures of Shark Bay and Exuma Cays. Generally, Feldman
and McKenzie (1998) proposed that in Exuma Cays stro-
matolites developed in intertidal settings, whereas
thrombolites are indicative of subtidal settings. A similar
depth-related succession was also discussed by Aitken
(1967). In contrast, at Shark Bay, non-laminated, irregular
thrombolytic clotted fabric of pustular mats indicate the
intertidal zone, while smooth mats with laminar parallel
layers are bound to the upper subtidal zone (Jahnert and
Collins 2013).
A Messinian counterpart from the Calcare di Base
Formation of the Caltanissetta Basin (Sicily) was described
Fig. 13 Peloidal grainstone with molluscs and intraformational
breccia (RA 4I): polished slab (a) showing alternation of mollusc-
and breccia-rich layers with peloidal grainstones; b–c: thin-sections
of the peloidal grainstone; the change from mollusc-rich grainstone
into pure peloidal grainstone is indicated by laminae, which are
interpreted as lithified microbial mats
440 Facies (2014) 60:429–444
123
by Oliveri et al. (2010). These stromatolites resemble the
Rabenkropf microbialites largely in geometry and dimen-
sion. Based on geochemical data, Oliveri et al. (2010)
proved that Messinian stromatolites had formed under
hypersaline conditions resulting from a low sea-level and
strong evaporation. Arenas and Pomar (2010) documented
a set of Late Miocene stromatolite-thrombolite units from
Mallorca (Spain) that formed during several transgressive
pulses, separated by short phases of emersion. This suc-
cession differs from the Rabenkropf section in its thickness
([30 m), the contribution by oolites and giant domal and
columnar bioherms that attain up to 5 m in height. Nev-
ertheless, the ‘‘undulate to flat-laminated non-oolitic stro-
matolites’’ and ‘‘domed non-oolitic stromatolites’’
(=UNOS and DNOS of Arenas and Pomar 2010) display
identical macro- and microstructures as recorded from the
Rabenkropf section. According to this concept, Ra 4A/B,
Ra 4C/D and partly 4F represent equivalents of the UNOS,
and Ra 4E, 4G and partly 4F are counterparts of low-relief
DNOS. Distorted stromatolitic fabrics, resembling
thrombolites but lacking well-developed mesoclots, as
observed in parts of Ra 4E, 4F, and 4G, is also typical for
the DNOS. At Mallorca, successions from UNOS to DNOS
are related to the initial transgressive pulses indicating the
transition from intertidal towards shallow subtidal condi-
tions. Large bioherm structures developed only during
subsequent deepening (Arenas and Pomar 2010). The
absence of such structures at the Rabenkropf section is thus
probably a result of limited accommodation space. This is
also reflected by the presence of cracks (Ra 4E, 4G),
contorted laminae and partly eroded laminae (Ra 4E) and
intraformational breccias (Ra 4E, 4H) pointing to repeated
periods of emersion and desiccation. The absence of for-
aminifers and grazing gastropods, as present in the bind-
stones at Ra CY (community building-yard), points to
extreme (e.g., hypersaline) environmental conditions. In
conclusion, the microbialite interval of the Rabenkropf
Section formed in a very shallow, probably hypersaline
lagoon; minor oscillations of the relative sea-level are
reflected by UNOS-DNOS-emersion successions (e.g., Ra
4A to 4E).
Post-microbialite interval: moderately agitated shallow
lagoon
The interpretation of the topmost part of the succession (Ra
4I) is limited by the poor preservation. The scree blocks of
grainstones and especially the topmost bed of peloidal
grainstones with numerous molluscs clearly indicate that
the main phase of stromatolite formation had ended—at
least in the exposed part of the section—and that ecological
conditions had improved. The mollusc fauna is low diverse
in species but individual-rich with masses of the mud
creeper Potamides nodosoplicatus. Extant Cerithideopsilla
conicus (Blainville, 1829), which is a modern counterpart
of P. nodosoplicatus, settles in estuarine, brackish-lagoonal
and hypersaline habitats where it forms huge populations in
the intertidal zone (Kowalke 2001; own observation M.H.).
Similarly, Potamides nodosoplicatus was reported from
Middle Miocene oolite shoals and littoral habitats from the
Eisenstadt-Sopron Basin (Harzhauser and Kowalke 2002)
as well as the Vienna Basin (Harzhauser and Piller 2010).
Similar assemblages with Diplodonta rotundata and pota-
mids were also reported from low-energy mudflats of late
Early Miocene age of the Paratethys (Zuschin et al. 2004).
Diplodonta rotundata still lives in the Mediterranean Sea
and the Eastern Atlantic where it is a shallow burrower in
muddy sand at sublittoral and shallow shelf depths (Oliveri
et al. 2010). Thus, the overall conditions seem to have been
similar to the pre-microbialite interval, but the lagoon was
slightly shallower and only moderately agitated.
Stromatolites recording the Badenian salinity crisis
The foraminifers of the Rabenkropf section allow a cor-
relation with the regional Spirorutilus Zone, which coin-
cides with the Middle Badenian of the Central Paratethys.
The absolute age and duration of this eco-biozone is still
poorly defined but the youngest age of the older Upper
Lagenidae Zone is constrained to \14.1 Ma by Hoheneg-
ger et al. (2012) while the younger Bulimina-Bolivina
Zone, marking the Late Badenian, correlates with the
nannoplankton Zone NN6, which starts at 13.6 Ma (Rogl
1998). This provides a rough time window of *0.5 Ma
and a latest Langhian age for the deposition of the Middle
Badenian transgressive–regressive cycle of Ritzing. This
phase coincides with the important Miocene Climate
Transition (Holbourn et al. 2007), which culminated in the
glacial event Mi-3b at 13.82 Ma (Abels et al. 2005) and a
major sea-level fall (Westerhold et al. 2005). In the Car-
pathian Foredeep and the Transylvanian Basin, this event
coincides with the onset of the Badenian salinity crisis,
which was dated by de Leeuw et al. (2010) at
13.81 ± 0.08 Ma. The duration of the event is estimated
by these authors to about 0.2–0.6 Ma. The Badenian
salinity crisis resulted in the accumulation of huge sulfate
and halite deposits (Peryt 2006; de Leeuw et al. 2010;
Babel et al. 2010). While carbonate stromatolites are
unknown from these basins, Peryt (2013) documented the
presence of gypsum stromatolites.
In contrast to the isolated Carpathian Foredeep and
Transylvanian Basin, the Pannonian Basin Complex was
still connected to the Mediterranean Sea via the Trans-
Tethyan Trench corridor (Rogl 1998; Piller et al. 2007).
Consequently, no gypsum and salt deposits formed in these
basins, where ‘‘normal’’ corallinacean platforms flourished.
Facies (2014) 60:429–444 441
123
Nevertheless, also the western basins of the Central Pa-
ratethys were severely influenced by the Miocene Climate
Transition and the related sea-level drop. The cooling of
the sea surface temperatures is reflected by the Mid-
Badenian extinction event (Harzhauser and Piller 2007),
which caused a decline in gastropod and foraminifer
diversity. Seismic data from the Vienna Basin indicate a
relative sea-level fall of about 90–120 m (Strauss et al.
2006), causing emergence of many early Badenian plat-
forms and the progradation of deltaic and lagoonal envi-
ronments far into the basins (Kovac et al. 2004).
Local record or regional pattern?
The described microbialites are not restricted to the Ra-
benkropf section, but can also be traced in small, aban-
doned, and nearly completely overgrown quarries in the
forests of Ritzing about 2.3 km WNW of the Rabenkropf
Section. These microbialites contain common mud-cree-
per gastropods (Granulolabium bicinctum) and suggest
less hostile conditions as represented by the top beds of
the section studied (Ra 4C–4H). The stromatolites of the
Rabenkropf section are located at an altitude of some
383 m a.s.l., while the other small occurrences in the
WNW are situated around 345 m a.s.l., which is related
to horst-graben-type extensional tectonics in this area
(Vendl 1933; Kishazi and Ivancsics 1977). These occur-
rences indicate that the formation of stromatolitic mi-
crobialites was widespread along the northern margin in
the Oberpullendorf Basin. Nevertheless, these stromato-
lites could still be interpreted as rather local phenomena
due to the virtual absence of similar late Langhian
(Middle Badenian) microbial deposits in other non-
evaporitic basins of the Paratethys Sea. Although this
view cannot be excluded, two factors should be kept in
mind. On the one hand, the recognition (and publication)
of such structures is still not common—e.g., the Ra-
benkropf section has been visited and described by sev-
eral mapping geologists and paleontologists (Janoschek
1931; Sieber 1956; Mostafavi 1978), but none of them
recognized the ‘‘unusual’’ carbonates as microbialites
until one of the authors (E.D.) identified them during a
fieldtrip based on his experience with Paleozoic micro-
bialites (Draganits and Noffke 2004). Similarly, Cornee
et al. (2009) suggested that microbial carbonates in
Badenian reefs might be quite common, but have been
overlooked in most Paratethyan outcrops. On the other
hand, the eustatic sea-level fall associated with the
Langhian-Serravallian boundary—or in other words the
Mi-3b glaciation—caused major erosion of coastal sedi-
ments in the entire Mediterranean-Paratethyan basins. The
preservation of littoral deposits of this phase is thus
limited to rare erosional relics. In several regions, such as
the adjacent Vienna Basin, no similar deposits can be
expected in surface outcrops as the middle Badenian sea-
level did not flood the early Badenian platforms (Strauss
et al. 2006). Potential equivalents might thus only be
preserved in subsurface outcrops, fringing the slopes of
these platforms.
Conclusions
During the middle Badenian transgression, the Oberpul-
lendorf Basin became flooded. In the investigated outcrops
at the northern part of the basin, after a short phase of
siliciclastic deposition, carbonate sedimentation started to
prevail in an open, moderately agitated lagoon with a
diverse mollusc fauna pointing to about 10–20 m water
depth. The phase of maximum transgression is only indi-
rectly documented by deep-burrowing Panopea shells in
underlying beds, while the coeval sediments became ero-
ded during subsequent exposure. Afterwards, a very shal-
low and hypersaline lagoon became established. Very soon
(within bed Ra 4A) the conditions became hostile for most
organisms aside from prokaryotes. A succession of flat-
laminated and undulate stromatolites towards low-relief
domal stromatolites developed. This succession indicates a
minor increase in accommodation space, but frequent tra-
ces of erosion, desiccation cracks, microbialite chips, and
intraformational breccias document repeated subaerial
exposure.
The mid-Badenian (late Langhian) age of the herein
described microbialites suggests a causal link of stromat-
olite growth with the onset of the Badenian salinity crisis.
Still active marine connections with the proto-Mediterra-
nean Sea and the different tectonic setting did not favor the
deposition of huge evaporites in the Pannonian Basin
Complex like in the Polish-Carpathian Foredeep and the
Transylvanian Basin. Instead, microbialites developed in
hypersaline lagoons of the Central Paratethys. Similar
stromatolite successions typically developed during the
latest Tortonian and Messinian in the proto-Mediterranean
Sea, heralding the Messinian salinity crisis. The phase of
stromatolite formation and evaporite deposition in the
Badenian of the Paratethys may thus be interpreted as
Middle Miocene analogue of the onset of the Late Miocene
Messinian salinity crisis.
Acknowledgments This study is a contribution to the FWF (Aus-
trian Science Fund) grant P-23492-B17. Many thanks to Markus
Reuter (University Graz) for discussions on carbonate ecology, to
Patrick Grunert (University Graz) for fieldwork, and to Alexander
Lukeneder (Natural History Museum Vienna) for fieldwork and out-
crop pictures. We thank Tadeusz M. Peryt (Polish Geological Insti-
tute, Warszawa) and Jose M. Martın (University of Granada, Spain)
for their careful reviews.
442 Facies (2014) 60:429–444
123
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