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ORIGINAL ARTICLE Stromatolites in the Paratethys Sea during the Middle Miocene climate transition as witness of the Badenian salinity crisis Mathias Harzhauser Jo ¨rn Peckmann Daniel Birgel Erich Draganits Oleg Mandic Do ¨rte Theobalt Julian Huemer Received: 6 October 2013 / Accepted: 28 November 2013 / Published online: 12 December 2013 Ó 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; Martı ´n et al. 1993; Martı ´n and Braga 1994; Braga et al. 1995; Calvet et al. 1996; Esteban 1996; Feldmann and McKenzie 1997; Braga and Martı ´n 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: [email protected] O. Mandic e-mail: [email protected] D. Theobalt e-mail: [email protected] J. Peckmann D. Birgel E. Draganits J. Huemer Department of Geodynamics and Sedimentology, University of Vienna, Althanstrasse 14, 1090 Vienna, Austria e-mail: [email protected] D. Birgel e-mail: [email protected] E. Draganits e-mail: [email protected] J. Huemer e-mail: [email protected] 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
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Stromatolites in the Paratethys Sea during the Middle Miocene ...

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Page 1: Stromatolites in the Paratethys Sea during the Middle Miocene ...

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: [email protected]

O. Mandic

e-mail: [email protected]

D. Theobalt

e-mail: [email protected]

J. Peckmann � D. Birgel � E. Draganits � J. Huemer

Department of Geodynamics and Sedimentology,

University of Vienna, Althanstrasse 14,

1090 Vienna, Austria

e-mail: [email protected]

D. Birgel

e-mail: [email protected]

E. Draganits

e-mail: [email protected]

J. Huemer

e-mail: [email protected]

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

Page 2: Stromatolites in the Paratethys Sea during the Middle Miocene ...

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

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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

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Page 4: Stromatolites in the Paratethys Sea during the Middle Miocene ...

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

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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

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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

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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

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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

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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

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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

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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

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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

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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

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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

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