www.geologicacarpathica.sk
GEOLOGICA CARPATHICA, APRIL 2010, 61, 2, 129—145 doi: 10.2478/v10096-010-0006-3
Upwelling conditions in the Early Miocene Central
Paratethys Sea
PATRICK GRUNERT
1
, ALI SOLIMAN
1
, MATHIAS HARZHAUSER
2
, STEFAN MÜLLEGGER
1
,
WERNER E. PILLER
1
, REINHARD ROETZEL
3
and FRED RÖGL
2
1
Institute for Earth Sciences (Geology and Paleontology), Graz University, Heinrichstraße 26, A-8010 Graz, Austria;
patrick.grunert@uni-graz.at; ali.soliman@uni-graz.at; stefan.muellegger@uni-graz.at; werner.piller@uni-graz.at
2
Natural History Museum Vienna, Geological-Paleontological Department, Burgring 7, A-1014 Vienna, Austria;
mathias.harzhauser@nhm-wien.ac.at; fred.roegl@nhm-wien.ac.at
3
Geological Survey of Austria, Neulinggasse 38, A-1030 Vienna, Austria; reinhard.roetzel@geologie.ac.at
(Manuscript received June 3, 2009; accepted in revised form October 2, 2009)
Abstract: Evidence for regional upwelling conditions in the Central Paratethys Sea is presented for mid-Burdigalian
(early Ottnangian) times. The oceanographic phenomenon is detected in clay-diatomite successions along the steep
escarpment of the Bohemian Massif in the eastern North Alpine Foreland Basin. Interpretations are based on a multi-
proxy data-set including published sedimentological and paleontological data, newly performed stable isotope measure-
ments (
δ
18
O,
δ
13
C) of foraminifers and bulk sediment samples, and analyses of dinoflagellate cyst assemblages. The
revealed stable isotope values of planktonic foraminifers point to upwelling: low
δ
13
C values indicate strong mixing of
surface waters with rising nutrient-rich waters, high
δ
18
O values reflect cool sea surface temperatures (SST). Tempera-
ture calculations give SSTs ranging from 10—14 °C. Cool SSTs and high productivity are additionally supported by bulk
sediment analyses. Assemblages of dinoflagellate cysts indicate a distal-shelf environment with nutrient-rich waters.
Westerly winds and tidal currents are discussed as potential driving forces behind the local upwelling event. As mid-
Burdigalian geography favoured strong current patterns in the Central Paratethys as documented in the sedimentary
record from the Rhône Basin to Hungary upwelling might have been a more common phenomenon in this epicontinental
sea than currently known.
Key words: Early Miocene, Central Paratethys, upwelling, foraminifers, dinoflagellates, stable isotopes.
Introduction
Coastal upwelling areas represent regions of the highest pri-
mary productivity in the world’s oceans. Warm surface wa-
ter currents caused by prevailing winds along a steep shore
are forced offshore due to the Coriolis effect triggered by
Earth’s rotation. The surface waters are replaced by rising
cold bottom waters bringing up high amounts of nutrients
which are usually stored at the sea floor (Summerhayes et al.
1995). The richness in nutrients triggers blooms of phy-
toplankton, providing the basis of a simple food web consist-
ing of zooplankton, fish swarms, sharks, whales and sea
birds (Lange et al. 1997; Granata et al. 2004). Much research
has been done on the causes and consequences of coastal up-
welling. By using many different techniques of oceanogra-
phy, studies have revealed detailed information about food
webs, hydrodynamics, sedimentation and biogeochemistry
(e.g. Lange et al. 1997; Nave et al. 2001; Granata et al. 2004;
Diz & Francés 2008; Salgueiro et al. 2008). It happens that
coastal upwelling can be triggered by different hydrodynamic
conditions. Besides wind patterns, tidal currents (e.g. Lee et
al. 1997) and topography (e.g. Oke & Middleton 2000) have
been discovered as potential driving and amplifying agents.
The information collected from extant upwelling sites is
used to trace back their history by documenting changes in
primary productivity and water temperature and thus in up-
welling intensity. These efforts have been quite successful
especially for the Pleistocene and have revealed links be-
tween changes in upwelling and global climate patterns (e.g.
Faul et al. 2000; Snyder et al. 2003; Nicholson et al. 2006).
However, detecting upwelling sites in vanished seas is still a
great challenge. Efforts from different disciplines of earth
sciences to find traces of upwelling in the geological record
have shown that this goal can only be achieved by a multi-
proxy approach combining various techniques of investiga-
tion (Peterson et al. 1995).
On the basis of sedimentological and micropaleontological
analyses, coastal upwelling has been repeatedly suggested
for the Early Miocene (mid-Burdigalian, early Ottnangian)
Central Paratethys Sea along the south-eastern margin of
the Bohemian Massif (Řeháková 1992, 1993, 1994, 1996;
Mandic et al. 2005; Roetzel et al. 2006). Based on this hy-
pothesis the present study offers new data from dinoflagel-
late cyst assemblages and geochemical measurements on
foraminifers and bulk sediment samples to address the ques-
tion of coastal upwelling in the area. The variety of proxies
revealed by this and previous studies will contribute to an in-
tegrated case study concerning upwelling events in the Cen-
tral Paratethys accompanied by a discussion of their
paleoceanographic plausibility.
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GRUNERT, SOLIMAN, HARZHAUSER, MÜLLEGGER, PILLER, ROETZEL and RÖGL
Geological setting
The early Ottnangian (mid-Burdigalian) Central Paratethys
paleogeography
The investigated outcrops are situated in the North Alpine
Foreland Basin of Austria and comprise Early Miocene sedi-
ments of the vanished epicontinental Central Paratethys Sea
(Roetzel et al. 1999b). The Central Paratethys came into exist-
ence around the beginning of the Oligocene when the rising
Alpine chains triggered a reorganization of paleo(bio)geo-
graphic patterns within the ancient Tethys Ocean (Rögl 1998;
Harzhauser & Piller 2007). Each of the resulting Mediterra-
nean, Central Paratethys and Eastern Paratethys Seas under-
went a history of its own. Thus, a regional stratigraphic
scheme was developed for each of them (see Piller et al. 2007
for details). Based on lithostratigraphy and biostratigraphic
evaluation of calcareous nannoplankton, diatoms, silicoflagel-
lates and foraminifers, the outcrops of this study are all regard-
ed as belonging to the early Ottnangian (mid-Burdigalian;
Fig. 1) (Roetzel et al. 2006; Rupp et al. 2008).
In the late Eggenburgian (ca. 19 Ma) a rapid transgression
connected the Western Paratethys again with the Central
Paratethys which led to the establishment of a new marine
pathway via the Alpine Foreland Basin into the Rhône Basin
(Fig. 2). This narrow connection is called the Burdigalian Sea-
way and persisted throughout the early Ottnangian (Rögl
1998). Sedimentation during the early Ottnangian was mainly
siliciclastic resulting in deposition of the characteristic sandy/
silty “Schlier” (Harzhauser & Piller 2007). Widespread tidal-
influenced deposits from Eggenburgian to early Ottnangian
are reported from the area of the Burdigalian Seaway (Home-
wood & Allen 1981; Allen & Homewood 1984; Allen et al.
1985; Faupl & Roetzel 1987, 1990; Keller 1989; Tessier &
Gigot 1989; Krenmayr 1991; Schaad et al. 1992; Martel et al.
1994; Salvermoser 1999; Bieg 2005). A frequent occurrence
of diatomites is documented for the North Alpine Foreland
Fig. 1. Lower Miocene stratigraphy for the Paratethys based on Piller et al. (2007). Black dot indicates stratigraphic position of the studied sec-
tions. Geochronology, geomagnetic polarity chrons, biozonations of planktonic foraminifers and calcareous nannoplankton after Lourens et al.
(2004), sequence stratigraphy and sea-level curve after Hardenbol et al. (1998) and oxygen isotope stratigraphy after Abreu & Haddad (1998).
Basin of Lower and Upper Austria and the Carpathians
(Kotlarczyk & Kaczmarska 1987; Kotlarczyk 1988; Roetzel et
al. 2006). Carbonate deposits like the bryozoan-corallinacean
limestones of the Zogelsdorf Formation in Lower Austria are
scarce (Piller et al. 2007).
This paleogeographic situation changed distinctly during
the late Ottnangian, when the seaways ceased and brackish
lakes developed in parts of the North Alpine Foreland Basin
and in the Carpathian Foredeep (Rögl 1998).
Regional geology
In the study area along the south-eastern margin of the
Bohemian Massif, Paleozoic rocks are overlain by Lower
Miocene marine nearshore sediments and a Pleistocene-Holo-
cene cover. The geological situation of this area is shown in
detail on the Austrian geological map GÖK22 Hollabrunn
(Roetzel et al. 1998; Fig. 3) and has been described by Roetzel
(1994, 1996, 2004) and Roetzel et al. (1999a).
The crystalline upland of the Bohemian Massif is bordered
against the Miocene sedimentary area in the east by the promi-
nent Diendorf fault zone, which is formed by NE-SW-running
subparallel dislocations with sinistral strike-slip character
(Roetzel 1996). The morphological slope consists of several
steep scarps, numerous spurs and frequent inselberg-like
bedrock elevations scattered across the foreland (Roštínský
& Roetzel 2005). Close to the main faults, both the crystalline
rocks and the bordering sediments of the foredeep are heavily
sheared and tectonically displaced.
The crystalline rocks of this area are mostly Paleozoic
granites and metamorphic rocks overlain by Lower Miocene
(upper Eggenburgian) nearshore sands and gravels of the
Burgschleinitz Formation. Above an erosional contact,
sandy shallow marine limestones of the Zogelsdorf Forma-
tion (lower Ottnangian) were deposited, which laterally and
vertically pass into deep-water pelitic sediments of the
Zellerndorf Formation. Drillings in this area show a thick-
131
EARLY MIOCENE UPWELLING IN THE CENTRAL PARATETHYS
ness of the pelites of about 25—100 m above the Zogelsdorf
Formation (Raschka 1912; Roetzel 1994, 1996). In the sur-
roundings of Limberg, Niederschleinz, Oberdürnbach, and
Parisdorf, very close to the Diendorf fault scarp, finely lami-
nated diatomites of the Limberg Member are intercalated
with the upper part of the Zellerndorf Formation, laterally
thinning out towards the east (Roetzel 1996; Roetzel et al.
1999b). In the area of Limberg—Parisdorf the diatomites are
at most 5—7.5 m thick. The overlying pelites of the Zellern-
dorf Formation consist of finely laminated and thin-bedded,
bluish-grey, light- and dark-brown, mostly non-calcareous
and smectitic silt-clays. They show calcareous layers only
immediately above the base of the Zogelsdorf Formation and
near the top above the Limberg Member. The Zellerndorf
Formation is discontinuously overlain by Lower-Middle
Miocene marine and freshwater sediments covered by Pleis-
tocene loess. Most of these formations east of the Diendorf
fault are affected by intensive horst-graben tectonics
(Fig. 3b).
Studied sites
As the succession of the Zellerndorf Formation and the in-
tercalated Limberg Member from the three investigated out-
crops has been described in detail in several earlier studies
(e.g. Roetzel et al. 1999b, 2006 and Mandic et al. 2005) only a
brief characterization of the localities is given here. Their geo-
graphic position and logs are shown in Figs. 3 and 4.
The small natural outcrop Niederschleinz is located in a
small ditch NW of the chapel of Niederschleinz. It exposes the
transition from pelites into the diatomites and is regarded as
representing a more distal facies of the Zellerndorf Formation
(Řeháková 1996; Roetzel 1996; Roetzel et al. 2006). Sample
NI 1 was taken here (BMN 716906/384548).
The Parisdorf diatomite pit is located 2.5 km ESE of Maissau
and about 400 m SE of Parisdorf. It belongs to the Wiener-
berger AG and is still in use. Diatomites are exposed at the
base, followed by pelites of the Zellerndorf Formation. Pelites
of the Zellerndorf Formation below the diatomites are known
from drillings and the surroundings of the pit which are poor in
fossils (Roetzel et al. 1999b). The Neogene sediments are cov-
ered by Pleistocene deposits. A detailed characterization of the
sediments and tectonics is given in Roetzel et al. (1999b, 2006).
For this study, samples PA 1—PA 8 were taken from the
pelites above the diatomites in the eastern part of the pit
(BMN 715067/380930—BMN 715075/380937). Additionally,
samples from earlier collections (1987, 1994) by R. Roetzel
were used for geochemical measurements: Sample 67-1 was
taken in the eastern part of the pit about 80 cm above the diato-
mite. Samples PAR-4 and PAR-5 are from the northern part at
about 3.7 m and 7.5 m above the diatomite and have been
studied for sedimentology and micropaleontology (calcare-
ous nannoplankton, foraminifers, diatoms, silicoflagellates)
by Roetzel et al. (2006). Their relative position to samples
PA 1—PA 8 is shown in Fig. 4.
The abandoned Limberg quarry is located NE of the railway
station, south of the road to Straning near the Taubenberg hill.
Similar to the Parisdorf pit, the finely stratified diatomites of
the Limberg Member are exposed at the base, followed by the
pelites of the Zellerndorf Formation. There is a sharp contact
between them with a distinct change of colour. The greyish
pelites are poorly stratified, and their base is non-calcareous.
Carbonate content increases upsection and calcareous concre-
tions occur irregularly. The benthic foraminifer Bathysiphon is
found frequently on the bedding planes. Strong tectonic defor-
mation such as in Parisdorf does not appear. For this study,
samples LI 1—LI 5 were taken from the pelites of the Zellern-
dorf Formation (BMN 716025/384618).
Material and methods
Dinoflagellates
Samples PA 1—PA 8 from Parisdorf and LI 1—LI 5 from
Limberg were processed according to standard palynological
techniques (Green 2001). A total of 12 rock samples, each
weighing 20—30 g, were cleaned, crushed and treated with
38% HCl (cold) to remove carbonates and 48% HF (cold) for
two days to remove silicates. The samples were rinsed to neu-
trality between each step and sieved through a 20 µm nylon
sieve (after ultrasonic treatment for 30 seconds). No heavy liq-
uid separation or oxidation treatment was applied. The residue
was washed and stained with Safranine “O”. Glass slides were
prepared from each sample using glycerin jelly and were
sealed with nail polish. At least two slides were scanned at a
magnification of 400
× for the productive samples using a Carl
Zeiss microscope (Axioplan 2) fitted with a Leica digital pho-
to camera DFC230. The first 250 dinocyst specimens of each
slide were counted and identified to species level whenever
possible. Additionally, observations and photographs were
made by using a DSM 982 Gemini SEM, operating at a work-
ing voltage of 10 to 15 kV.
Fig. 2. Paleogeographic sketch-map for the early Ottnangian cir-
cum-Mediterranean area based on Rögl (1998). The asterisk indi-
cates the study area. E.P. = Eastern Paratethys.
132
GRUNERT, SOLIMAN, HARZHAUSER, MÜLLEGGER, PILLER, ROETZEL and RÖGL
Fig. 3. Geological map (A) and cross-section (B) of the study area. Arrows in (A) indicate the studied sections Parisdorf, Niederschleinz
and Limberg. Modified from Roetzel et al. (2006).
133
EARLY MIOCENE UPWELLING IN THE CENTRAL PARATETHYS
Stable isotopes
Sample preparation
All samples were dried at 35 °C. 100g of each sample
were soaked in diluted H
2
O
2
as earlier studies have shown
that H
2
O
2
does not alter the isotopic composition of foramin-
iferal tests (Ganssen 1981). Samples were then wet sieved
under running water and separated into four size-fractions:
63—150 µm, 150—300 µm, 300—600 µm and > 600 µm. The
sieved fractions were first put into deionized water and then in
undenatured Ethanol.
Thereafter the washed samples were dried at 35 °C again,
clean tests of the chosen planktonic and benthic foraminifers
were picked from fractions 63—150 µm and 150—300 µm of
samples NI 1, PA 1—PA 3 and PAR-4. Between 18 and 55
tests were selected for each measurement, depending on par-
ticular species and size. Selected specimens from all the inves-
tigated samples were studied under the SEM to exclude a
possible influence of diagenesis. All the other samples yielded
no (PA 4—PA 8, LI 2, LI 3) or badly preserved and/or diage-
netically altered (LI 1, LI 5, PAR-5) specimens.
Fig. 4. Logs of the studied sections Parisdorf, Limberg and Nieder-
schleinz.
Isotopic composition of bulk sediment samples PA 1—PA 8,
PAR-4, PAR-5, 67—1, LI 1—LI 3 and LI 5 was measured twice
for each sample. Therefore sediment of each sample was
crushed and homogenized in a mortar.
To compare the revealed bulk sample signal, 24 samples
(OS 1—24) from the Ottnangian stratotype section Ottnang-
Schanze in Upper Austria have been processed in the same
way and were included in the analysis. These sediments are
dated to early Ottnangian and are described in Rögl et al.
(1973) and Rupp et al. (2008).
Selected foraminiferal species
As mixed-layer dwelling Globigerina bulloides is common-
ly used for isotopic analysis it seemed reasonable to pick
closely related Globigerina lentiana and Globigerina praebul-
loides from all suitable samples (Fig. 5). Additionally, Globi-
gerina ottnangiensis was picked from sample PAR-4.
Besides globigerinids, mass occurrences of small microper-
forate tenuitellids characterize the samples (Roetzel et al.
2006). Although not commonly used in isotopic studies and
thus expected to be difficult to interpret, specimens of Tenuitel-
la clemenciae were picked from sample PA 1 in order to pro-
vide additional planktonic data.
Selecting benthic foraminifers was limited by the fact that
the samples usually contained very small specimens showing
high species diversity but low total numbers. Thus, only infau-
nal species Bulimina striata striata, Melonis pompilioides,
Myllostomella advena, Myllostomella recta, Pullenia bul-
loides and Siphonodosaria consobrina were picked from sam-
ples NI 1 and PAR-4. Although their isotopic signal was
expected to be influenced by synsedimentary pore water, a
comparison of the two samples should be possible after care-
ful consideration of vital effects.
Stable isotope measurements
Isotopic analyses on foraminifers and bulk sediment sam-
ples from NI 1, PA 1—PA 8 and LI 1—LI 5 were performed at
the Institute of Earth Sciences at the University of Graz, using
an automatic Kiel II preparation line and a Finnigan MAT
Delta Plus mass spectrometer. Samples were dried and reacted
with 100% phosphoric acid at 70 °C. Analytical precision,
based on replicate analysis of international standards NBS-19
and NBS-18 and an internal laboratory standard is better than
0.08 ‰ for
δ
18
O and 0.04 ‰ for
δ
13
C. Results are reported
in conventional
δ notation relative to the Vienna Pee Dee
Belemnite standard (VPDB) in ‰ units.
Foraminifers from NI-1 and PAR-4 as well as the bulk sedi-
ment samples from Ottnang-Schanze were measured for
δ
13
C
and
δ
18
O values at the Joanneum Research in Graz. The setup
of the analytical system combines a continuous-flow isotope-
ratio mass spectrometer (Finnigan DeltaplusXP) with a Ther-
moFinnigan GasBench II equipped with a CTC Combi-Pal
autosampler. A comparable experimental setup has been used
in other studies (Spötl & Vennemann 2003). The samples and
two international reference materials (NBS-19, IAEA-CO-8)
were simultaneously analysed by using the phosphoric acid
method at a T = 75 °C. The isotope values of the samples are
134
GRUNERT, SOLIMAN, HARZHAUSER, MÜLLEGGER, PILLER, ROETZEL and RÖGL
given relative to the VPDB-standard (Coplen 1996). For rep-
licate measurements of different aliquots of samples the
overall error of reproducibility is < 0.15 ‰ (VPDB) for both
δ
13
C and
δ
18
O values.
Results
Dinoflagellates and other palynomorphs
The investigated samples PA 8 from Parisdorf and all
Limberg samples revealed dinoflagellate cysts (Table 1). The
dinoflagellate cysts are well preserved but the assemblages are
rather poor and dominated by few taxa. The samples mainly
consist of Cleistosphaeridium spp. together with common oc-
currences of Lingulodinium machaerophorum, Operculodinium
centrocarpum, Lejeunecysta spp. and Brigantedinium spp.
Besides dinocysts, other palynomorphs have been encoun-
tered in samples PA 8 and LI 1—LI 5 consisting of sporomorphs
(Pinus, Cathaya, Abies, Picea, Acer) and the prasinophycean
chlorophyte Pterospermella. In samples LI 1 and LI 2 organ-
ic wall morphotypes resembling Glomus have been found in
considerable numbers (Fig. 6.9—12). All other samples are
barren of palynomorphs.
Stable isotopes
Foraminifers
The results for all 19 measurements are summarized in Ta-
ble 2.
δ
18
O values for all planktonic foraminifers are negative
and vary between —1.46 ‰ and —0.56 ‰. With respect to glo-
bigerinids, G. lentiana always shows slightly higher values
than G. praebulloides of the same test size and sample (mean
offset: + 0.12 ‰ for fraction 150—300 µm; + 0.09 ‰ for frac-
tion 63—150 µm). G. ottnangiensis shows significantly lower
values in sample PAR-4 than G. praebulloides. T. clemenciae
revealed the highest value (—0.76 ‰) within sample PA 1.
δ
13
C values for planktonic tests are also negative in all sam-
ples ranging from —1.52 ‰ to —0.03 ‰. G. lentiana shows on
average slightly lower values in their
δ
13
C signal than G.
praebulloides of the same test size and sample values (mean
offset: —0.29 ‰ for fraction 150—300 µm; —0.05 ‰ for frac-
tion 63—150 µm). An offset between larger and smaller tests in
G. lentiana (mean: + 0.13 ‰) and G. praebulloides (mean:
+ 0.34 ‰) can be observed for all the samples. T. clemenciae
shows the highest value (—0.8 ‰) within sample PA 1.
With respect to benthic foraminifers, Siphonodosaria con-
sobrina from sample NI 1 revealed the only positive values in
all measured species and thus shows highest values in both
δ
18
O and
δ
13
C (0.72 ‰ and 0.47 ‰). Myllostomella recta oc-
curs in both samples and shows the most negative
δ
18
O and
δ
13
C values of all benthic species. A significant offset of at least
—1 ‰ for both values from all other benthic species is docu-
mented. The intra-specific offset in M. recta between samples
NI 1 and PAR-4 is —0.29 ‰ in
δ
18
O and —1.02 ‰ in
δ
13
C.
Bulk samples
Bulk samples for Parisdorf show negative
δ
18
O values rang-
ing from —5.81 ‰ to —2.57 ‰ (Table 3). Whereas samples
PA 1—PA 7, PAR-4, PAR-5 and 67—1 range within a mean
offset of 1.2 ‰ without showing a clear trend, sample PA 8
differs at least in one measurement very distinctly.
The
δ
13
C-record for the bulk samples revealed values
ranging from —0.99 ‰ to + 0.09 ‰ for Parisdorf. Samples
Fig. 5. Studied planktonic foraminifers. 1 – Globigerina praebulloides, sample PA 1, 450
×; 2 – Globigerina lentiana, sample PA 1,
250
×; 3 – Globigerina ottnangiensis, sample PAR-4, 250×; 4 – Tenuitella clemenciae, sample PA 1, 400×.
Samples
Species
PA 8 LI 1 LI 2 LI 3 LI 5
Cleistosphaeridium spp.
a a a a a
Lingulodinium machaerophorum
c c c a
Spiniferites/Achomosphaera spp.
r r r
Lejeunecysta spp.
c c r
Brigantedinium spp.
s c
Operculodinium centrocarpum
s r c
Trinovantedinium sp.
s
Pentadinium laticinctum
s r
Pterospermella spp.
r
c
Pollen
a a a c a
Fungal
spores
c a c c c
Table 1: Dinoflagellate cysts and other palynomorphs revealed
from the studied Limberg (LI) and Parisdorf (PA) samples. The
first 250 specimens were counted from each sample. Abundant (a):
> 20; common (c): 5—20; rare (r): 2—4; single (s): 1.
135
EARLY MIOCENE UPWELLING IN THE CENTRAL PARATETHYS
PAR-5 and PA8 yielded the lowest values, the later was ab-
errantly low (—8.55 ‰).
Niederschleinz revealed values similar to Parisdorf ranging
from —33 ‰ to —91 ‰ for
δ
18
O and —62 ‰ to —46 ‰ for
δ
13
C.
The samples from Ottnang-Schanze show values from
—5.47 ‰ to —3.96 ‰ (mean: —4.88 ‰) and
δ
13
C values ranging
from —0.25 ‰ to + 0.69 ‰ (mean: + 0.26 ‰).
Discussion
Dinoflagellates
Recent upwelling areas are known to be dominated by hetero-
trophic dinoflagellates which feed on the highly abundant
diatoms (e.g. Zonneveld et al. 2001; Sprangers et al. 2004).
Frequent taxa reported from areas of seasonal coastal up-
welling include Brigantedinium spp., Operculodinium centro-
carpum, Lingulodinium machaerophorum and different
Spiniferites species (De Vernal & Marret 2007), all of which
are present in the samples of this study.
Several studies have shown that the presence of Lingulo-
dinium machaerophorum in shelf sediments correlates with
nutrient enriched waters (e.g. Wall et al. 1977; Dale 1996;
Targarona et al. 1999). In the current study, the occurrence of
L. machaerophorum is in some samples positively correlated
with the abundance of protoperidinioid dinoflagellate cysts as
Lejeunecysta, Brigantedinium and Trinovantedinium which
also indicate elevated nutrient levels (e.g. Wall et al. 1977;
Bujak 1984; Lewis et al. 1990; Powell et al. 1990).
Table 2:
δ
18
O and
δ
13
C values of the planktonic and benthic foraminifers measured within the present study. All isotopic values are given
in ‰ VPDB.
Locality Sample
Species
Grain-size
fraction
No.
δ
18
O
δ
13
C
Planktonic foraminifers
Parisdorf PA
1
Globigerina lentiana
150–300 27
–1.36
–1.50
Globigerina praebulloides
150–300 25
–1.43
–1.22
Globigerina lentiana
63–150
45
–0.99
–1.52
Globigerina praebulloides
63–150
55
–1.08
–1.40
Tenuitella clemenciae
63–150
46
–0.76
–0.80
PA
2
Globigerina praebulloides
63–150
50
–1.46
–1.35
PA
3
Globigerina lentiana
150–300
30
–0.67
–0.9
Globigerina praebulloides
150–300 30
–0.95
–0.84
Globigerina lentiana
63–150
34
–0.72
–1.15
Globigerina praebulloides
63–150
50
–0.81
–1.18
PAR-4
Globigerina ottnangiensis
150–300 30
–1.40
–0.32
Globigerina praebulloides
150–300 40
–0.56
–0.03
Benthic foraminifers
Niederschleinz NI
1
Bulimina striata striata
150–300 35
–0.28
–0.35
Melonis pompilioides
150–300 19
–0.48
–0.34
Myllostomella recta
63–150
33
–1.82
–1.39
Pullenia bulloides
150–300 20
–0.45
–1.07
Siphonodosaria consobrina
150–300
25
0.72
0.47
Parisdorf PAR-4
Myllostomella advena
63–150
42
–1.16
–1.46
Myllostomella recta
63–150
51
–2.11
–2.41
Locality Sample
δ
18
O
δ
13
C
Parisdorf
PA 1
–3.5
–1.09
PA 2
–3.3
–0.53
PA
3
–2.65
–0.65
PA
4
–3.12
–0.53
PA
5
–3.08
–0.35
PA
6
–2.77
0.03
PA
7
–2.88
–0.37
PA 8
–4.5
–3.79
PAR-4
–3.01
–0.79
PAR-5
–3.73
–2.72
67–1
–3.11
–0.44
Limberg LI
1
–3.47
–0.89
LI
2
–2.22
0.37
LI
3
–4.08
–3.69
LI 5
–6.9
–8.55
Niederschleinz NI
1
–3.12
–0.54
Ottnang–Schanze OS
1
–4.79
–0.08
OS 2
–5.31
–0.2
OS 3
–5.11
0.4
OS
4
–4.83
0.02
OS
5
–4.81
0.06
OS 6
–5.1
–0.25
OS
7
–4.93
0.22
OS
8
–4.83
0.12
OS
9
–4.95
0.26
OS
10
–5.13
–0.16
OS
11
–3.96
0.32
OS
12
–4.84
0.27
OS
13
–5.15
0.57
OS
14
–4.64
0.69
OS
15
–4.63
0.68
OS 16
–5.24
0.5
OS
17
–4.98
0.19
OS
18
–4.76
0.34
OS
19
–5.11
0.17
OS
20
–5.47
0.32
OS
21
–4.42
0.57
OS
22
–4.53
0.51
OS 23
–4.8
0.46
OS
24
–4.71
0.36
Table 3:
δ
18
O and
δ
13
C values of the bulk samples measured within
the present study. All isotopic values are given in ‰ VPDB.
136
GRUNERT, SOLIMAN, HARZHAUSER, MÜLLEGGER, PILLER, ROETZEL and RÖGL
The dominant taxon in the studied assemblages is Cleisto-
sphaeridium. Although common in the fossil record, the pa-
leo-autecology of this genus is still poorly understood.
According to Brinkhuis (1994) and Sluijs et al. (2005) high
numbers of C. placacanthum, C. ancyreum and C. diversis-
pinosum suggest a distal shelf environment.
An estimation of sea-surface temperatures is not possible
as the encountered dinocysts occur over a very broad range
of temperatures. For example, recent L. machaerophorum is
a temperate to tropical, euryhaline species present in regions
where water-temperature ranges from —1.5 °C winter SST to
29.1 °C summer SST (Marret & Zonneveld 2003).
Some specimens of Lingulodinium machaerophorum with
reduced processes (Fig. 6.2—3) have been revealed from the
lower part of the Limberg section. The occurrence of such
morphotypes has often been linked to reduced salinity (Head
et al. 2005; Head 2007). However, a major change in salinity
seems unlikely for the studied sections as the stable isotope
data clearly contradict this idea by showing no distinct trend.
Other palynomorphs
Pollen of Pinus, Cathaya, Abies, Picea and Acer as well as
fungal spores of Glomus have been encountered in the stud-
ied samples (Table 1). Given the idea of a distal upwelling
setting as indicated by dinoflagellate cysts and mass occur-
rences of planktonic foraminifers (Roetzel et al. 2006), their
occurrence appears enigmatic at first. However, palynologi-
cal studies have shown that pollen grains can be transported
by winds and ocean currents dozens of kilometers off the
coast (e.g. Hooghiemstra et al. 2006). As strong winds and
current patterns are dominant features of upwelling sites, an
aeolian transport of the herein revealed pollen seems most
likely. Input by river-transport can be excluded as freshwater
indicators like the algae Pediastrum are absent in all samples
(whereas marine prasinophyceaean algae are present) and no
river sediments are known from the study area.
Recent Glomus is associated with plant roots and synony-
mized with the fossil fungal spore Palaeomyces. The uncom-
pressed nature, clustering and abundance of arbuscular
mycorrhizal hyphae preserved in the association together
with the outcrop situation strongly point to a post-deposi-
tional origin of these fungal spores.
Planktonic foraminifers
Stable isotope values of globigerinid foraminifers as indi-
cator for coastal upwelling
Surface waters in upwelling areas show a characteristic
isotopic signal (e.g. Steens et al. 1992; Wefer et al. 1999;
Peeters et al. 2002): high
δ
18
O values reflect low tempera-
tures, low
δ
13
C values result from strong mixing with cold
nutrient-rich deeper waters depleted in
13
C. This characteristic
isotopic composition should be reflected in tests of organ-
isms which calcify in such an environment. A number of
studies have shown this with recent and fossil foraminifers
(e.g. Faul et al. 2000; Peeters et al. 2002).
The results of the globigerinid foraminiferal tests in the
present study show values that are in good agreement with
coastal upwelling:
δ
18
O values vary between —46 ‰ and
—56 ‰,
δ
13
C ratios range from —1.52 ‰ to —0.03 ‰. When
the data are plotted together with Miocene to recent data of
the same or closely related species (Vergnaud-Grazini
1978; Šutovská & Kantor 1992; Pearson et al. 1997; Faul et
al. 2000; Peeters et al. 2002; Báldi 2006), a relation with
upwelling areas is obvious (Fig. 7). This plot also shows
that in fact the carbon isotope values are the main indicator
for upwelling as they point to mixing of the surface water
with nutrient rich bottom water. Temperature is known to
be one of the most important factors for the distribution of
foraminifers (Schiebel & Hemleben 2005). Therefore, tests
of the same species from different areas should provide
similar
δ
18
O values. Fig. 7 shows this effect for G. praebul-
loides from our Ottnangian samples and the samples of
non-upwelling areas in the Central Paratethys, the Mediter-
ranean and the Atlantic seas (Vergnaud-Grazini 1978;
Šutovská & Kantor 1992; Pearson et al. 1997).
Low
δ
13
C ratios can also be caused by freshwater input of
nearby rivers. This is very unlikely for the present case as
there is no evidence of an ancient river in the sedimentary
record around the study area. Additionally, the fresh water
influx would distinctly lower oxygen isotope values.
Sea surface temperatures
As
δ
18
O ratios are mainly determined by water temperature,
they can be used to calculate absolute water temperatures. The
classic notation for this purpose was defined by Epstein et al.
(1953) based on molluscs. Up to now, several equations for
tests of different benthic and planktonic foraminifers were de-
veloped (see Bemis et al. 1998 for a summary). The notation
of Shackleton (1974) based on uvigerinids has become the
most popular:
T = 16.9—4.38x(
δ
18
O
c
—
δ
18
O
w
) + 0.1x(
δ
18
O
c
—
δ
18
O
w
)
2
(1)
where T is temperature in °C,
δ
18
O
c
the composition of the
shell carbonate and
δ
18
O
w
is the composition of the water in
which the carbonate was precipitated.
Species specific vital effects result in offsets in the isotopic
composition of the test compared to the surrounding water
(e.g. Peeters et al. 2002). The problem with extinct foraminifers
is that the influence of vital effects on their shell composition
remains unknown. One possibility to deal with this problem is
an actualistic approach.
The globigerinids used in this study, Globigerina lentiana
and Globigerina praebulloides, are both closely related to
Globigerina bulloides (Kennett & Srinivasan 1983). There-
fore, the use of the equation developed by Bemis et al. (1998)
seems more reasonable for calculating water temperatures
from these species:
T=13.2—4.89x(
δ
18
O
c
—
δ
18
O
w
)+ 0.27x(
δ
18
O
c
—
δ
18
O
w
)
2
(2)
All temperature equations take into account the
δ
18
O com-
position of the surrounding seawater (
δ
18
O
w
). Today the sea-
137
EARLY MIOCENE UPWELLING IN THE CENTRAL PARATETHYS
Fig. 6. Dinoflagellate cysts and fungal spores. Photomicrographs are bright field (1—9) and scanning electron microscope (10—15); scale bar is
20 µm except where noted: 1 – Lejeunecysta paratenella; dorsal view, sample LI 2; slide B; England Finder T45. 2—3,10 – Lingulodinium
machaerophorum; 2—3 – uncertain orientation of the same specimen with short processes (bulbous); different foci; sample LI 2; slide B (2—3);
uncertain orientation of specimen with long processes; sample PA 8 (10). 4 – Pterospermella sp., sample LI 3, slide B, England Finder K38.
5 – Spiniferites sp., sample LI 3, slide B, England Finder S34/4. 6—7 – Pentadinium laticinctum, sample LI 1, slide C, England Finder S51,
?ventral view different foci. 8 – Clusters of Cleistosphaeridium spp.; sample PA 8; slide B. 9, 12 – Glomus spp., sample LI 1; slide B;
England Finder J39 (9) and SEM from sample PA 8 (12). 11 – Cleistosphaeridium diversispinosum; uncertain orientation; sample PA 8.
13—14 – Cleistosphaeridium ancyreum; specimen in apical view (9) showing the archeopyle; sample PA 8 (9) and uncertain orientation of
specimen from sample PA 8. 15 – Cleistosphaeridium placacanthum; oblique apical view; sample PA 8.
138
GRUNERT, SOLIMAN, HARZHAUSER, MÜLLEGGER, PILLER, ROETZEL and RÖGL
water has a mean
δ
18
O composition of 0 ‰ (SMOW), but this
value can vary locally due to evaporation or mixing with fresh
water. For example, a
δ
18
O
w
of + 1 ‰ is reported for the Medi-
terranean (Pierre 1999) and + 2 ‰ for the Red Sea (Craig
1966). Thus,
δ
18
O
w
-values are not the same for all oceans
and they are not constant in time. Lear et al. (2000) suggest a
globally averaged
δ
18
O
w
of ca. —1 ‰ for the Early Miocene
based on Mg/Ca ratios of benthic foraminifers. Harzhauser
et al. (2007) showed that this value is in good agreement
with Early Miocene mollusc data from the Central Para-
tethys. As all results of this study are given relative to VPDB,
the
δ
18
O
w
value has to be converted to VPDB by —0.27 ‰ ac-
cording to Hut (1987).
Based on these assumptions, temperature estimates for globi-
gerinid species vary between 10—14 °C for an assumed
δ
18
O
w
of
—1 ‰ in most samples from the Parisdorf section which is in
good accordance with reported estimates based on micro-
faunal assemblage composition (Table 4; Roetzel et al. 2006).
For reasons of comparison, temperatures were also calcu-
lated with the commonly used equation established by
Shackleton (1974). The resulting values exceed the calcula-
tions based on Bemis et al. (1998) by 3—4 °C and clearly
contradict all other proxies (Table 4). As this equation has
been derived from benthic uvigerinids, its application to
planktonic foraminifers seems inappropriate.
Depth habitats
As water temperature decreases with depth,
δ
18
O data can
be used to determine depth habitats for different species of
foraminifers (Niebler et al. 1999). In the present study,
Tenuitella clemenciae from sample PA 1 shows the highest
values (—0.76 ‰; mean offset to all globigerinids from the
Parisdorf section: + 0.46 ‰; mean offset to globigerinids
with test size 0.063 µm: + 0.28 ‰) indicating that this spe-
cies lived deeper in the water column than the globigerinids.
This corresponds well with published data of recent tenuitel-
lids (Li et al. 1992, 1999).
Fig. 7.
δ
18
O vs.
δ
13
C plot of the globigerinids (Globigerina lentiana, G. ottnang-
iensis, G. praebulloides) from the Ottnangian samples compared to data-sets
from recent upwelling and non-upwelling areas. Numbers in brackets give sieved
fraction in µm; isotopic values are given in ‰ VPDB. Data for Arabian Sea from
Peeters et al. (2002), Eastern Pacific from Faul et al. (2000), Tengelic-2 (Hunga-
ry) from Báldi (2006), LKŠ-1 (Slovak Basin) from Šutovská & Kantor (1992),
DSDP-data (Mediterranean) from Vergnaud-Grazini (1978) and ODP-data
(Atlantic) from Pearson et al. (1997).
Benthic foraminifers
As benthic foraminifers occupy ecological
niches on and within the sediment their
geochemical signal is influenced by the pore-
water circulating in the sediment. This “micro-
habitat-effect”
has
been
documented
in
countless studies and can alter the
δ
13
C signal
significantly compared to the
δ
13
C of bottom
water dissolved inorganic carbon (
δ
13
C
DIC
; e.g.
Mackensen et al. 2000; Fontanier et al. 2006).
Additionally, as in planktonic foraminifers, the
geochemical signal in benthic foraminifers is al-
tered by diverse vital effects. Thus, a summary
of the current knowledge on the geochemistry
and ecology of the benthic species referred to in
this study is given in Table 5 together with the
corrected isotopic values for the different benth-
ic foraminifers and for Globigerina praebul-
loides from this study.
For sample NI 1, the corrected values fit quite
well, especially for the
δ
18
O values. Assuming
that the corrected
δ
18
O values for B. striata stri-
ata, M. pompilioides and P. bulloides (mean:
—0.07 ‰) represent bottom water conditions we
can assume a correction factor of + 1.75 ‰ for
Myllostomella recta resulting of —0.36 ‰ for
sample PAR-4. The slight offset of + 0.45 ‰ to
the corrected G. praebulloides-value of the same
sample indicates a low temperature gradient and
strong mixing of the water column. Applying the
above-mentioned equation of Shackleton (1974)
based on Uvigerina (which is supposed to be in
equilibrium with bottom waters) calculations sug-
gest 11—12 °C bottom water temperature for
Niederschleinz and 13 °C for Parisdorf (Table 4).
The ecological preferences of the investigated
taxa clearly point to high productivity in the up-
per water-column: e.g. Melonis and Bulimina are
regarded as “high-productivity” taxa (Caralp
139
EARLY MIOCENE UPWELLING IN THE CENTRAL PARATETHYS
Table 4: Temperature calculations from tests of the planktonic foraminifers Globigerina lentiana and G. praebulloides and benthic fora-
minifers based on the equations of (1) Shackleton (1974) and (2) Bemis et al. (1998). A value of —1 ‰ is assumed for
δ
18
O
w
according to
Harzhauser et al. (2007). For details see text.
Sample Species
Grain-size
fraction
δ
18
O T
(°C)
1
T
(°C)
2
Planktonic foraminifers
PA 1
PA 1
PA 1
PA 1
PA 2
PA 3
PA 3
PA 3
PA 3
PAR-4
Globigerina lentiana
Globigerina praebulloides
Globigerina lentiana
Globigerina praebulloides
Globigerina praebulloides
Globigerina lentiana
Globigerina praebulloides
Globigerina lentiana
Globigerina praebulloides
Globigerina praebulloides
150–300
150–300
63–150
63–150
63–150
150–300
150–300
63–150
63–150
150–300
–1.36
–1.43
–0.99
–1.08
–1.46
–0.67
–0.95
–0.72
–0.81
–0.56
17
18
16
16
18
14
16
15
15
14
14
14
12
12
14
10
12
11
11
10
Benthic foraminifers
NI 1
PAR-4
Bulimina striata striata
Melonis pompilioides
Pullenia bulloides
Myllostomella recta
150–300
150–300
150–300
63–150
–0.18
0.02
–0.05
–0.36
12
11
12
13
–
–
–
–
Table 5: Microhabitat effect of the stable isotope
composition of the studied benthic foraminifers
and Globigerina praebulloides as revealed by dif-
ferent studies. In case of more than one correction
value a mean value was calculated. Asterisks indi-
cate estimates based on the genus level. Only large
tests of G. praebulloides were used except for
sample PA 2. References: (1) Naidu et al. (2004);
(2) Mackensen et al. (2000); (3) McCorkle et al.
(1990); (4) Grossman (1987).
1989; Murray 2006; Smart et al. 2007). As the studied fora-
minifers are the most abundant benthic species within the
samples their stable isotope signals seem to be reliable and
in good accordance with a proposed upwelling setting.
The bulk sample record
Recent studies have shown that bulk sediment signal
roughly reflects the isotopic composition of coccoliths and
thus gives additional information about surface water condi-
tions (e.g. Minoletti et al. 2001; Kováčová et al. 2008). In-
fluence of meteoric and pedogenic diagenesis is reflected in
aberrantly light isotope values (Armstrong-Altrin et al.
2009). Thus, Parisdorf samples PAR-5 and PA 8 as well as
all Limberg samples are excluded from analysis.
For the Lower Austrian study area the remaining samples
show rather similar values without a distinct trend (mean
values: —3.05 ‰/—0.52 ‰; Fig. 8). Compared to Ottnang-
Schanze with mean values of —4.88 ‰ and + 0.26 ‰, both
signals show a clear offset ( + 1.75 ‰ for
δ
18
O/—0.78 ‰ for
δ
13
C; Fig. 9). The higher
δ
18
O and lower
δ
13
C thus point to
lower SSTs and higher bioproductivity for Parisdorf and
Niederschleinz.
The multi-proxy approach
Only a multi-proxy approach can lead to a reliable identifi-
cation of upwelling events in the sedimentary record (Peterson
et al. 1995). Consequently, all available data from the herein
studied sections shall be discussed in particular for coastal up-
welling (see Table 6 for a summary).
Upwelling conditions for the Zellerndorf Formation and the
diatomitic Limberg Member were originally suggested on the
basis of microfossil analyses (Řeháková 1994, 1996; Mandic
et al. 2005; Roetzel et al. 2006): assemblages of calcareous
nannoplankton, diatoms, silicoflagellates, sponge spicules and
foraminifers point to a nutrient-rich, highly productive envi-
ronment. SST-estimates range from 10—15 °C. The isotopic
data revealed in the present study fit very well with these
proxies.
Referring to paleobiogeography, Roetzel et al. (2006)
pointed out that the composition of foraminiferal communi-
ties in the study area differs clearly from the common early
Ottnangian assemblages described from Upper Austria
(Rupp et al. 2008) and Bavaria (Wenger 1987) indicating
special oceanographic conditions.
On the macrofossil level, palm leaves (Berger 1955), fish
(Bachmayer 1974), insects (Bachmayer 1974), birds (Bach-
mayer 1980), crabs (Bachmayer 1983) and bladder wrack
(Mandic et al. 2005) have been documented for the Limberg
Member from different localities in Lower Austria. Plant de-
bris and fish teeth have been reported from the Zellerndorf
Formation in the Parisdorf pit (Mandic et al. 2005). With re-
spect to environmental conditions, the high number of fish
remains (scales and teeth as well as whole specimens) indi-
cates a very productive setting attracting fish swarms. Layers
Species
δ
18
O–δ
18
O
eq
δ
13
C
DIC
Sample δ
18
O
corr
δ
13
C
corr
Ref.
Globigerina praebulloides
Bulimina striata striata
Melonis pompilioides
Pullenia bulloides
+0.25 *
–0.1 *
–0.5
–0.4
–0.8 *
–0.3
PA 1
PA 2
PA 3
PAR-4
LI 1
NI 1
NI 1
NI 1
–1.68
–1.71
–1.20
–0.81
–2.53
–0.18
+0.02
–0.05
–
–
–
–
–
–
–0.04
–
1
2, 3
4
4
140
GRUNERT, SOLIMAN, HARZHAUSER, MÜLLEGGER, PILLER, ROETZEL and RÖGL
Fig. 8. Trends in
δ
18
O and
δ
13
C revealed from bulk samples (solid
lines) and planktonic foraminifers for the Parisdorf section. Dotted
line shows trend for Globigerina praebulloides.
with masses of fish scales are also a typical feature in coeval
well-cores and point to a widespread phenomenon (personal
observation F. Rögl). Two brachyuran specimens assigned to
the family Geryonidae by Bachmayer (1983) are also of inter-
est, since extant species of this family are known as deep-sea
crabs living on the shelf break and continental slope down to
depths of 3800 m (Jones et al. 2003). Some geryonid species
have been described from upwelling areas off Baja California
(Pleuroncodes planipes) and Angola (Geryon maritae)
(Walsh et al. 1974; Bianchi 1992).
Based on the faunal and floral data, upwelling is assumed
for the pelites as well as for the intercalated diatomites. Con-
cerning the change in sedimentation, sedimentological data
presented by Roetzel et al. (1999b) suggest that the input of
volcanic ash further amplified the bloom of diatoms leading to
a further boost in primary productivity by bringing additional
silica in the system and thus resulting in the deposition of the
diatomites (Mandic et al. 2005; Roetzel et al. 2006).
The driving agent
Having a handful of proxies available suggesting upwelling
along the south-eastern margin of the Bohemian Massif dur-
ing the early Ottnangian, the fit with the paleogeographic and
paleoceanographic framework has to be discussed. At first
thought an upwelling setting in the narrow epicontinental
Central Paratethys Sea seems unlikely. Today, the most prom-
inent coastal upwelling areas are situated along the coasts of
Africa, South America, Australia and the Arabian Peninsula
providing a steep continental slope of several thousand meters
(Summerhayes et al. 1995). This was not the case in the shal-
low Central Paratethys as Roetzel et al. (2006) suggest a deep
sublittoral environment for the Lower Austrian study area.
However, they point out similarities in topography: the steep
paleocoast along the Bohemian Massif triggered by the Dien-
dorf fault resembles the steep continental slope on a smaller
scale (Fig. 3). The modern upwelling in the narrow Santa
Barbara Channel along the coast of California might serve as
an analogue (Lange et al. 1997; Hendershott & Winant 1996):
restricted by a chain of islands, it reaches depths of approxi-
mately 500 m at its deepest part in the Santa Barbara Basin.
Given a suitable topography a driving force behind the sug-
gested upwelling is still in question. Two main agents have
been identified to trigger extant upwelling (e.g. Lee et al.
1997; Oke & Middleton 2000): tidal currents and prevailing
winds producing surface currents. Sea floor and basin topog-
raphy can further amplify these currents. Both scenarios can
be applied to the Early Miocene Central Paratethys.
(1) In most cases upwelling is a wind-driven phenomenon.
Thus, as suggested by Roetzel et al. (2006), prevailing wester-
ly winds blowing parallel to the ancient coastline along the
Bohemian Massif might thus have induced surface currents
resulting in the coastal upwelling setting (Fig. 10A).
(2) Widespread meso- to macrotidal deposits are document-
ed throughout the Central Paratethys during early-mid Burdi-
galian ranging from the French, Swiss and German Molasse
(Homewood & Allen 1981; Allen & Homewood 1984; Allen
et al. 1985; Keller 1989; Tessier & Gigot 1989; Lesueur et al.
1990; Schaad et al. 1992; Martel et al. 1994; Salvermoser
Fig. 9. Comparison of
δ
18
O and
δ
13
C for bulk sediment samples
from Lower and Upper Austria. Note that the samples PAR-5 and
PA 8 and all Limberg samples are not included due to diagenesis.
141
EARLY MIOCENE UPWELLING IN THE CENTRAL PARATETHYS
Table 6: Synopsis of all available sedimentological, biogenic and geochemical data reported in literature and in this study for the Zellerndorf
Formation and the Limberg Member. References: (1) Roetzel et al. (2006); (2) Mandic et al. (2005); (3) Roetzel et al. (1999); (4) Řeháková
(1996, 1994, 1993, 1992); (5) Bachmayer (1983, 1980, 1974). For more references and a detailed discussion see text.
Proxy Remarks
Reference
1) Sediment
diatomites and pelites of the Zellerndorf Fm
2) Biota
foraminifers
diatoms
calcareous nannoplankton
silicoflagellates
dinoflagellates
macrofossils
3) Geochemistry
δ
18
O and δ
13
C from planktonic and benthic
foraminifers
diatomites finely laminated; commonly known from upwelling areas
planktonics point to cold, nutrient-rich surface waters; blooms of cold-water
tenuitellids; benthics depend on high organic flux from surface waters
frequent occurrence of Thalassionema nitzschioides characteristic of nutrient-rich,
high productive areas; absence of shallow-water benthic taxa
blooms of Coccolithus pelagicus with an optimal growth temperature of 2–12 °C
frequent occurrence of cold and temperate taxa
neritic, nutrient-elevated environment
fish, deep-sea crabs; insects, birds, palm leaves, bladder wreck
rather high δ
18
O values and low δ
13
C values point to cold, nutrient-rich environment
and low water-column stratification
1, 2, 3, 4
1, 2
1, 2, 4
1, 2
1
this study
2, 5
this study
Fig. 10. Illustrations for the two discussed upwelling scenarios. A – Upwelling driven by prevailing westerly winds. B – Upwelling driv-
en by meso- and macroscale tidal currents. For details see text.
1999; Bieg 2005) via the Austrian North Alpine Foreland
Basin (Faupl & Roetzel 1987, 1990; Krenmayr 1991) to the
North Hungarian Bay (Sztanó 1994, 1995; Sztanó & De Boer
1995). These strong tidal currents supposedly amplified by the
narrow paleogeography of the region are considered as possi-
ble driving forces for Paratethyan upwelling (Fig. 10B).
The paleogeography of the Early Miocene Central Para-
tethys with its narrow, long-stretched foreland basins favoured
amplification of current patterns during phases of open con-
nections to the Mediterranean (Allen et al. 1985; Bieg 2005).
Such conditions existed several times from Egerian to early
Ottnangian giving a time frame for possible upwelling events
(Rögl 1998; Harzhauser & Piller 2007). Massive diatomites
intercalated with pelites, commonly seen as indicator of up-
welling conditions (Wagner 1998; Mandic et al. 2005), are
not only known from the localities of this study. Time equiv-
alent Early Miocene diatomites are also reported from the
Carpathian Foredeep in Moravia and Poland (Kotlarczyk &
Kaczmarska 1987; Kotlarczyk 1988; Picha & Stráník 1999).
The widespread distribution of diatomites in the Early Mi-
ocene of the Central Paratethys might indicate that upwelling
events were more common in the Central Paratethys than
currently known.
Conclusions
A multi-proxy data-set from diatomite-clay successions in
the North Alpine Foreland Basin of Lower Austria consisting
of sedimentological and paleontological data from earlier
142
GRUNERT, SOLIMAN, HARZHAUSER, MÜLLEGGER, PILLER, ROETZEL and RÖGL
studies, stable isotope analyses of foraminiferal shells and
bulk sediment samples as well as dinoflagellate assemblages in-
dicate upwelling conditions along the margin of the Bohemian
Massif in the Central Paratethys during mid-Burdigalian
times. Planktonic foraminifers examined for their isotopic
composition show low
δ
13
C values and rather high
δ
18
O values,
being remarkably consistent with data from recent upwelling
areas. Temperature calculations based on globigerinids re-
vealed sea surface temperatures from 10 to 14 °C. Low SSTs
and high productivity are supported by the bulk sample
record. Benthic foraminifers point to a low temperature gradi-
ent and strong mixing of the water column. Dinoflagellate as-
semblages indicate a highly productive, distal environment.
The influence of NE trade winds and strong tidal currents are
discussed as potential driving agents of the herein studied up-
welling site. Coeval mid-Burdigalian deposits with marine di-
atomites are widespread in the Paratethys Sea from Austria
and Moravia up to Poland. The local upwelling setting along
the steep coast of the Bohemian Massif might thus reflect a
characteristic hydrodynamic and/or wind regime along the
Paratethyan coasts between ca. 19—18 Ma.
Acknowledgments: We want to thank Albrecht Leis (Johanne-
um Research, Graz) for carrying out part of the isotopic mea-
surements. We are grateful to Fabrizio Lirer (Istitutio per
l’Ambiente Marino Costiero, Naples, Italy), Michal Kováč
(University of Bratislava, Slovakia), Andrea Kern (University
of Vienna), Andreas Kroh and Oleg Mandic (both Natural His-
tory Museum Vienna) for many helpful discussions. Martin
Head (Brock University, St. Catharines, Canada) and Lilian
Švábenická (Czech Geological Survey, Prague) are thanked for
constructive comments which helped to improve the paper.
Franz Topka (Natural History Museum Vienna) is thanked for
assisting with the fieldwork. Financial support for this study was
provided by the Commission for the Palaeontological and Strati-
graphical Research of Austria (Austrian Academy of Sciences).
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Appendix
Faunal reference list of the identified foraminifers and dinoflagellate cysts. Taxonomy of the Foraminifera follows Cicha et
al. (1998) and Roetzel et al. (2006), dinoflagellate cyst nomenclature is based on Fensome et al. (2008). Descriptions and
representative illustrations can be found in the same publications.
Foraminifera
Bulimina striata striata D’Orbigny 1837
Globigerina lentiana Rögl 1969
Globigerina ottnangiensis Rögl 1969
Globigerina praebulloides Blow 1959
Melonis pompilioides (Fichtel & Moll 1798)
Myllostomella advena (Cushman & Laiming 1931)
Myllostomella recta (Palmer & Bermudez 1936)
Pullenia bulloides (D’Orbigny 1826)
Siphonodosaria consobrina (D’Orbigny 1846)
Tenuitella clemenciae (Bermudez 1961)
Dinoflagellate cysts
Achomosphaera ramulifera (Deflandre) Evitt 1963
Cleistosphaeridium ancyreum (Cookson & Eisenack) Eaton et al.
2001
Cleistosphaeridium diversispinosum Davey et al. 1966 emend. Eaton
et al. 2001
Cleistosphaeridium placacanthum (Deflandre & Cookson) Eaton et al.
2001
Lejeunecysta paratenella (Benedek 1972) Artzner & Dörhöfer 1978
Operculodinium centrocarpum (Deflandre & Cookson) Wall 1967 s.l.
Pentadinium laticinctum Gerlach 1961 emend. Benedek et al. 1982