ROGGENDORF-1, A KEY-SECTION FOR STRATIGRAPHIC POSITION OF GRUND FORMATION 165
GEOLOGICA CARPATHICA, 55, 2, BRATISLAVA, APRIL 2004
165178
ROGGENDORF-1 BOREHOLE, A KEY-SECTION FOR
LOWER BADENIAN TRANSGRESSIONS AND THE STRATIGRAPHIC
POSITION OF THE GRUND FORMATION (MOLASSE BASIN,
LOWER AUSTRIA)
STJEPAN ÆORIÆ
1
and FRED RÖGL
2
1
Department of Paleontology, University of Vienna, Althanstrasse 14, A-1090 Vienna, Austria; stjepan.coric@univie.ac.at
2
Museum of Natural History Vienna, Burgring 7, A-1014 Vienna, Austria; fred.roegl@nhm-wien.ac.at
(Manuscript received June 5, 2003; accepted in revised form December 16, 2003)
Abstract: Borehole Roggendorf-1 was drilled in the Alpine-Carpathian Foredeep (Molasse Basin) north of the Danube
(Lower Austria). Biostratigraphic results and the lithological column revealed until now unrecorded Early Badenian
(Middle Miocene) cycles. Calcareous nannoplankton was studied from the upper 800 m of a Neogene sequence and
foraminifers were examined from the upper 410 m. The upper 2 m to 255 m fine clastic sediments of the Grund Forma-
tion (Lower Badenian, nannoplankton Zone NN5, planktonic foraminiferal Zone Mt6) show a deepening upward, with a
maximum depth corresponding to outer shelf. Paleoecological evaluations demonstrate a distinct warming of the surface
water. Down-hole, a clastic sequence follows starting with a gravel bed (347360 m), and ending with a conglomerate
bed on top (255270 m). The latter is probably the transgressive base of the Grund Formation. The boundary of nanno-
plankton Zones NN 4NN5 lies within this earlier Badenian cycle, which was deposited on the inner shelf, below 50 m.
Limestone and sandstone pebbles originate from the Calcareous Alps and Flysch Unit. The underlying cycle of calcare-
ous silty shales, sands and thin gravel layers belongs to the Laa Formation (Karpatian, nannoplankton Zone NN4; 360
612 m). Deposition occurred, partly under dysoxic bottom conditions on the outer shelf to upper bathyal. Surface waters
were distinctly cooler than in the Grund Formation due to strong upwelling with nutrient enrichment. The Karpatian is
underlain without a distinct unconformity by the Upper Ottnangian brackish Rzehakia (Oncophora) Beds, fine sands
and shales, which are barren of fossils (612678 m). The lower part of the investigated section belongs to the Ottnangian
Robulus Schlier. Nannoplankton determinations show that this still belongs to nannoplankton Zone NN4. Nanno-
plankton Zone NN3/4 is recorded on the basis of the occurrence of Sphenolithus belemnos only in the lowermost samples
(790800 m).
Key words: Miocene, Alpine-Carpathian Foredeep, Grund Formation, Laa Formation, paleoecology, biostratigraphy,
microfossils.
the Rzehakia Beds in the thrust. The late Early Miocene (Kar-
patian/Late Burdigalian) Laa Formation transgressed discor-
dantly on older surfaces. At the beginning of the Middle Mi-
ocene the Badenian Sea transgressed from the southeast
(comp. Jiøíèek 2001; Jiøíèek & Seifert 1990; Stráník &
Brzobohatý 2000).
The Lower Badenian sediments, developed in northern Aus-
tria as sequences of marls, silts, sands, and gravels, belong to
the time-equivalent Grund and Gaindorf Formations. The
Mailberg Formation consists of corallinacean limestone with
some marly intercalations. The submarine fan of the Hollen-
burg-Karlstetten Formation, coming from the Alps in the
southwest, interfingers with the Gaindorf Formation. The geo-
logical situation of the study area (Fig. 1) is described in detail
by Roetzel et al. (1999) and Roetzel & Pervesler (2004).
The basal Badenian sediments in the foredeep have been
dated by calcareous nannoplankton as nannoplankton Zone
NN4. Nannoplankton Zone NN5 and, based on the occurrence
of Praeorbulina glomerosa circularis, planktonic foraminifer-
al Zone M5b are recorded in the Grund Formation (Rögl et al.
2002; Rögl & Spezzaferri 2003; Spezzaferri 2004). This con-
trasts with the interpretation of Cicha (1999a), vábenická &
Ètyroká (1999), and vábenická (2002), who placed the lower
Introduction
Different Miocene formations are exposed in the Austrian Mo-
lasse Basin north of the Danube. Miocene sequences in the
deep drilling Roggendorf-1 were investigated to determine the
stratigraphic extension of the Badenian Grund Formation.
Roggendorf-1, drilled by OMV AG in 1962, penetrated
1008 m of Neogene sediments, and terminated in a volcano-
clastic complex of the Gresten Formation (Jurassic).
Geological setting
The Austrian Molasse Basin, as part of the Alpine-Car-
pathian Foredeep, changes direction in the investigated area
from a west-east stretching basin to northeast, following the
outline of the Bohemian Massif (Fig. 1). Marine sedimenta-
tion started north of the Danube in the Egerian (Late Oli-
gocene to Early Miocene). Lower Miocene (Eggenburgian to
Ottnangian) marine sediments follow concordantly. The facies
changed to brackish Rzehakia (Oncophora) Beds, ending
the first Lower Miocene marine cycle. Overthrust of Alpine-
Carpathian nappes narrowed the basin strongly, and included
166 ÆORIÆ and RÖGL
part of the Grund Formation in the Early Miocene Karpatian
Stage.
Lithology of borehole Roggendorf-1
The lithology is based on an internal report of OMV AG
(Schulz 1966), on the resistance log, and on the washed resi-
due of cutting samples (Fig. 2). Samples were available from
the upper 10 m, and from 130 m downward. The upper 2 m of
the section belong to Quaternary soil and loess.
2255 m. Lower Badenian, Grund Formation: Light brown
to grey-green, silty to sandy, micaceous marly shales, with in-
tercalated layers of fine to coarse sands and fine gravels. In the
fine fraction of the residue, angular quartz and mica dominate,
and in the coarse fraction quartz, crystalline and carbonate
Fig. 1. Geological sketch of the Alpine-Carpathian Foredeep in
northeastern Austria, and position of the investigated site Roggen-
dorf-1, together with drill sites NÖ-06 Gneixendorf, 2 and NÖ-07
Diendorf near Hadersdorf am Kamp (redrawn acc. Kreutzer 1993).
grains are present. Some pyrite concretions and lignitic plant
remains occur. The foraminiferal fauna is abundant in the up-
permost part (samples 210 m) only.
255360 m. Lower Badenian, basal clastic sequence:
255270 m. Conglomerates and sandstones: gravels and
pebbles of grey, dark grey and grey-brown limestone and do-
lomite, light brown biogeneous and oolitic limestones, blue-
grey chert, hard sandstones, some quartz and crystalline peb-
bles, originating mainly from the Calcareous Alps and Flysch
Unit. Greenish-grey calcareous sandstones are intercalated,
partly also as matrix of the conglomerate.
270347 m. Fine sands and silty shales: greenish-grey and
light grey, silty and sandy, micaceous calcareous shales with
interbedded layers of grey fine sand, sometimes coarse sand
and small gravels. In the fine residue, mainly angular quartz,
in the coarse fraction well-rounded quartz, carbonates, hard
sandstone and some crystalline pebbles, lignitic plant remains,
and rare pyrite occur. Strong reworking of foraminifers is ob-
served; autochthonous foraminiferal assemblages are scarce.
347360 m. Basal gravels: commonly quartz, crystalline
components rare; grey, dark grey, black, and brownish car-
bonates, and light brown and grey, biogenous limestones; hard
fine-grained sandstones. Carbonates and sandstones originate
from the Alps.
360612 m. Karpatian, Laa Formation: grey and greenish-
grey, silty to sandy micaceous calcareous shales, alternating
with layers of grey fine sand, and a few horizons with gravels.
The fine fraction of the residue consists of quartz and grey car-
bonates, in the coarse fraction are rounded grains of quartz,
crystalline, carbonate, and sandstone. Some pyrite concretions
and common lignitic or coal particles occur. The gravels and
coarse sands consist of well-rounded quartz, some crystalline,
sandstone, and a few carbonates. In cuttings of 370 m the resi-
due consists similarly of quartz and carbonate, and pyritized
diatoms are present as in the following samples. Because of
the presence of diatoms the upper boundary of the Karpatian
has been placed at the base of the gravel bed at 360 m.
612678 m. Ottnangian, Rzehakia (Oncophora) Beds:
grey fine sands with layers of dark grey, well-bedded clay, and
a layer of light grey calcareous sandstone at 652 m. The bi-
valve Rzehakia (Oncophora) was not recorded. The correla-
tion is based on lithology and geophysical measurements.
678800 m (end of investigation). Ottnangian, Robulus
Schlier:
678715 m. Dark greenish-grey, silty-sandy shales with
thin beds of fine sand, and with fish and molluscan remains,
along with some foraminifers.
715735 m. Greenish-grey, clayey fine sand with layers of
dark shales; with some foraminifers, mainly Lenticulina
(Robulus).
735780 m. Greenish-grey sand and grey clayey glauconitic
sandstone with pyrite concretions. Some molluscan and echi-
noid remains, rare foraminifers.
780793 m. Coarse sand and gravel, well rounded, domi-
nated by quartz; with thin layers of shales. With few mol-
luscan and echinoid remains.
793800 m. Alternating layers of sand, glauconitic sand-
stone, and greenish-brownish grey sandy shales. Some fish
and molluscan remains, rare foraminifers.
ROGGENDORF-1, A KEY-SECTION FOR STRATIGRAPHIC POSITION OF GRUND FORMATION 167
Material and methods
The calcareous nannofossil distribution in Roggendorf-1
was studied from the upper 800 m of the section. Samples
from the interval 10130 m were not available. Smear slides
were prepared for all samples and analysed using a light mi-
croscope (1000
×
magnification) at normal and crossed nicols
to identify calcareous nannofossils. Statistical methods were
applied to quantitative data using the Software PRIMER 5
(Clarke & Warwick 1994). This method was already success-
Fig. 2. Borehole Roggendorf-1: stratigraphy, lithology, resistivity, abundance patterns of selected calcareous nannofossils, the percent-
age of reworked nannoplankton, and variations in C. pelagicus/R. minuta ratio (Cp/Rm).
168 ÆORIÆ and RÖGL
fully applied for the paleoecological interpretation of the mid-
dle Karpatian from Laa an der Thaya, Lower Austria (Spezza-
ferri & Æoriæ 2001). Square-root transformed abundances
were used for hierarchical agglomerative clustering (Group
Average Linking) based on the Bray-Curtis Similarity coeffi-
cient (Fig. 3). Barren samples were not included. Samples are
ordered by non-metric MultiDimensional Scaling (nMDS) on
the basis of the same similarity matrix as in the clusters, which
are investigated through the Similarity and Dissimilarity Term
Analysis.
The foraminiferal fauna has been qualitatively investigated
from cuttings between 2 and 410 m for biostratigraphic and
paleoecological indications.
Results
Paleoecology
Calcareous nannoplankton
The autochthonous calcareous nannofossil distribution in
Roggendorf-1 borehole is arranged alphabetically and listed
in Appendix A.
The data on calcareous nannoplankton were quantitatively
analysed using the Bray-Curtis Similarity. Based on agglom-
erative clustering it is possible to distinguish 6 classes (Ap-
pendix C, Figs. 3, 4a).
The Similarity and Dissimilarity Term Analyses of calcare-
ous nannoplankton (Appendix C) suggest that Cluster 2
groups assemblages, which are characterized by a high per-
centage of Reticulofenestra minuta. This species accounts for
89.5 % of the average similarity within this cluster. This clus-
ter includes only samples of Badenian age belonging to the
NN5 Zone (Fig. 4b,c). Cluster 6 groups samples, which indi-
cate high nutrients and coastal upwelling, are characterized by
Coccolithus pelagicus and Syracosphaera pulchra. These two
species account for 57 % of the average similarity. Clusters 2
to 5 are characterized by the stepwise increase in the ratio of
C. pelagicus at the expense of R. minuta. In Cluster 1 two spe-
cies (C. pelagicus and R. minuta) account for 66.7 % of the
Fig. 3. Hierarchical agglomerative clustering based on the Bray-
Curtis Similarity of calcareous nannofossils from Roggendorf-1.
average similarity. These samples are characterized by a very
low abundance of calcareous nannofossils and therefore can-
not be satisfactorily interpreted. According to these data it is
possible to interpret the first axis of the nMDS as a nutrient
(Figs. 4bc) and surface water temperature gradient (Fig. 4a).
Clusters 1, 5 and 6 group samples containing only typical
Karpatian sediments from the NN4 Zone. Clusters 3 and 4 in-
clude samples from the Ottnangian to Badenian without dis-
tinct preference (Fig. 4b,c).
The sample from 510 m contains a calcareous nannofossil
assemblage with a high percentage (27.7 %) of Braaru-
dosphaera bigelowii. This nannofossil association is charac-
terized by a reduced diversity and contains a relatively high
percentage of Coccolithus pelagicus and Syracosphaera pul-
chra. Reticulofenestra minuta, Reticulofenestra sp., R. gelida,
Helicosphaera carteri and Sphenolithus moriformis are rare.
Braarudosphaera bigelowii is very scarce or absent in other
samples. Nagymarosy (1991) described a Braarudosphaera-
bloom from Oligocene sediments and explained it with the
partial separation of the Paratethys. vábenická (1999) report-
ed Braarudosphaera-rich sediments in the Turonian of the
Bohemian Cretaceous Basin. Bukry (1974) used the high per-
centage of Braarudosphaera bigelowii in Holocene sediments
from the Black Sea as an indication of low marine salinity.
The enrichment of this cold, nutrient-rich-water-loving spe-
cies in sediments from Roggendorf-1 suggests a short period
of fresh water input and reduced salinity of the surface waters.
Winter et al. (1994) concluded that availability of nutrients,
light and temperature are the factors which control phy-
toplankton productivity. Coccolithus pelagicus belongs to the
group of so-called r-strategists, which are characteristic of nu-
trient-rich eutrophic environments. The water movements in
upwelling areas lead to enhanced nutrient availability. Such
habitats within the euphotic zone were typical for Karpatian
sediments within the NN4 Zone. Sparser nutrient supplies
during the Badenian (nannoplankton Zone NN5) created
oligotrophic conditions within a well-stratified water column
and enabled the R. minuta-bloom (Fig. 4b,c). Hallock (1987)
pointed out that oligotrophic biotas feature small-sized phy-
toplankton and longer, more complex food chains. Ottnangian
sediments from the NN4 Zone recorded in Roggendorf-1
show more oligotrophic paleoceanographic characteristics,
whereas the 800 m sample (NN3NN4) has more eutrophic
features.
The paleoecological interpretation of the calcareous nanno-
fossil assemblages is based on variations in the abundances of
C. pelagicus and R. minuta. Coccolithus pelagicus is already
well known as an important paleoclimatic marker. This spe-
cies is normally used as a paleotemperature proxy for cooler
waters. It is abundant at water temperatures between 1.5 and
+15 °C, with optimum growth from 2 to 12 °C (Okada &
McIntyre 1979; Winter et al. 1994). The enrichment of C. pe-
lagicus in sediments indicates high nutrient levels in surface
water and upwelling paleoconditions. Beaufort & Aubry
(1992) studied abundance variations of C. pelagicus at the
Kerguelen Plateau (Southern Indian Ocean) within the Ocean
Drilling Program (ODP) Site 747A. They computed the per-
centage of C. pelagicus vs. Reticulofenestra spp. and com-
pared their results with paleoceanographic events revealed by
stable isotope studies.
ROGGENDORF-1, A KEY-SECTION FOR STRATIGRAPHIC POSITION OF GRUND FORMATION 169
4a. Arrangement of clusters shows the increase from cooler to warmer
conditions.
4b. Changes in trophic conditions. Eutrophic surface waters dominate
in the Karpatian; during the Badenian a progressive decrease of nutrient
supply occurs, whereas the Ottnangian shows intermediate trophic con-
ditions.
4c. Changes in trophic conditions in nannoplankton Zones NN3NN5.
Fig. 4. Non-metric MultiDimensionalScaling (nMDS) of calcare-
ous nannofossils from Roggendorf-1.
According to the Cp/Rm ratio (C. pelagicus/(number of R.
minuta + C. pelagicus)) the following subdivision of the bore-
hole Roggendorf-1 is proposed (Fig. 2):
1. The interval from 2 m to 270 m with very low values of
Cp/Rm % (up to 20 %), which generally corresponds to sedi-
ments of the Grund Formation. Low percentages of Cocco-
lithus pelagicus and the bloom of Reticulofenestra minuta
characterize this interval. It is interpreted as showing the in-
fluence of warm waters without upwelling conditions. Dis-
coasterids have a rare and sporadic occurrence in the upper
part of this interval only.
2. The interval from 270 m to 360 m shows a stepwise in-
crease of this value from about 10 % at 270 m to about 80 %
at 320 m. This clastic part of the section is characterized by a
continuous increase in abundance of C. pelagicus, and can be
regarded as the transitional horizon between the Laa and Grund
Formations. It indicates a gradual change in paleoecological
conditions.
3. The interval from 360 m to 570 m is characterized by
very high abundances of C. pelagicus (up to more than 90 %).
Such an increase corresponds to strong upwelling conditions.
4. The interval from 570 m to 730 m is barren of calcare-
ous nannofossils and includes the lowest part of the Laa For-
mation, Rzehakia Beds, and the upper part of the Robulus
Schlier.
5. The interval from 730 m down to 800 m shows a repeat-
ed increase of C. pelagicus in thanatocoenoses.
Changes in the paleoenvironment are clearly expressed by
the distribution of samples in the non-metric MultiDimension-
al Scaling plots (Fig. 4b,c). There is a clear distinction be-
tween eutrophic and oligotrophic patterns within time. The
lowermost Ottnangian sample (800 m) belonging to the nan-
noplankton Zone NN3/NN4 shows eutrophic conditions. In-
termediate surface water masses existed in the later Ottnan-
gian (Fig. 4b,c). An upwelling system with eutrophic
conditions dominated during the Karpatian, while in the Bad-
enian a gradual change to warmer and more oligotrophic con-
ditions in surface waters occurred. The most oligotrophic con-
ditions existed in the warm period of the Grund Formation.
Note also that reworked nannofossil species are significant-
ly more abundant in the Karpatian and lowermost Badenian,
which is caused by strong erosion and turbulent water masses.
Abundance changes of reworked species are presented in Fig.
2. The correspondence of this abundance pattern to the Cp/
Rm ratio is obvious. Strong reworking of mostly Cretaceous
species is observed, e.g. Watznaueria barnesae, Micula de-
cussata, Arkhangelskiella cymbiformis, Eiffellithus gorkae,
Eiffellithus turriseiffelli, Cribrosphaerella ehrenbergii. Re-
worked Paleogene species are represented by: Chiasmolithus
altus, Reticulofenestra bisecta, R. stavensis, R. umbilica, R.
hillae, Ericsonia spp., Toweius spp. etc.
Foraminifers
In the Grund Formation (2255 m), the uppermost 10 m of
the section contain the richest foraminiferal assemblages, de-
creasing in abundance down-section. The distribution of spe-
cies is given in Appendix B. Lagenids are common, whereas
agglutinated foraminifers and miliolids are scarce. The plank-
tonic assemblage is dominated by small globigerinas; Globi-
gerinoides occurs regularly, orbulinids are very scarce, while
170 ÆORIÆ and RÖGL
small globorotalias (G. bykovae) are abundant. The occur-
rence of Globigerinoides and Globorotalia indicates warm
surface waters. The benthic assemblage is characteristic for
the outer shelf. The reduction of diversity and the increase of
Ammonia in the lower part point to shallower conditions, than
in the upper part and thus a deepening upward of the section.
Higher numbers of Valvulineria complanata in some layers
indicate a reduced oxygen content in the bottom sediments. A
gradual enrichment of the assemblages towards the top of the
formation is shown by Cicha (1999b).
Clastic Sequence (255360 m): The gravels and conglom-
erates at 255270 m are barren. In the finer clastics, autochth-
onous foraminifers are mainly small globigerinas and small
benthics. Richer assemblages at 320330 m with Amphimor-
phina, Caucasina, Hanzawaia, Heterolepa, Mylostomella,
and Pseudoparrella indicate deeper water, at least below
50 m, and the accompanying Ammonia, Elphidium, and Po-
rosononion may be transported from shallow regions. The
high content of reworked specimens from the Upper Creta-
ceous and Paleogene in the clastic sequence is remarkable.
The basal gravels are barren.
Laa Formation (360612 m): A distinct faunal change is
observed at 370 m, with an increase of small, five-chambered
globigerinas and some deep-water agglutinated forms (Bathy-
siphon, Haplophragmoides). This indicates water depth of
outer shelf to upper bathyal and cooler surface waters for the
upper part of the Karpatian section. The foraminiferal fauna is
scarce or samples are barren, with the increase of sand down-
section. From the lower part some Ammonia beccarii are re-
ported, which indicate shallower water. Pyritized foraminifers
and the common occurrence of pyritized diatoms indicate dys-
oxic bottom conditions. Some reworking of Upper Cretaceous
foraminifers and recrystallized radiolarians is observed.
According to internal reports (Schulz 1966; Fuchs 1963)
the Rzehakia Beds are barren, and the upper part of the Rob-
ulus Schlier (678715 m) contains commonly fish remains
and foraminifers (Cyclammina, Lenticulina, lagenids, cibic-
ids). In the sandy part of the section some molluscan and echi-
noid detritus occurs with a scarce foraminiferal assemblage
(Cyclammina?, Haplophragmoides, lagenids, Lenticulina,
Bulimina aculeata, Siphonina, Heterolepa dutemplei, Nonion,
Elphidium). This indicates greater water depth (outer shelf)
with a transport from shallow areas.
Biostratigraphy
Calcareous nannoplankton
Miocene sediments from Roggendorf-1 generally contain
well-preserved calcareous nannofossil assemblages. Samples
350, 470 and 540 m and the interval from 590 m to 710 m are
barren of nannofossils. The biostratigraphically important
species Sphenolithus heteromorphus is very scarce but
present in the whole section. The absence of Helicosphaera
ampliaperta and the scarce presence of S. heteromorphus in
the upper part of the section Roggendorf-1 (from 7 to 320 m)
indicate the Sphenolithus heteromorphus Zone (nannoplank-
ton Zone NN5). The accompanying assemblage is character-
ized by the presence of small helicoliths (H. walbersdorfensis
and H. vedderi), H. carteri, H. waltrans, Coccolithus pelagi-
cus, Coronocyclus nitescens, Cyclicargolithus floridanus,
Discoaster formosus, D. musicus, D. variabilis, Reticu-
lofenestra daviesii, R. gelida, R. haqii, R. minuta, Spheno-
lithus moriformis, Syracosphaera pulchra, Thoracosphaera
spp., and Umbilicosphaera jafarii.
Investigations of calcareous nannofossils from the Mühl-
bach Beds, Gaindorf Formation, Lower Badenian (Æoriæ
2003) and the Karpatian-Badenian transition in the Styrian
Basin showed that H. waltrans occurs only in nannoplankton
Zone NN5. This corresponds to the distribution pattern in Mi-
ocene sediments of the Mediterranean region (Fornaciari et al.
1996). They confirmed that Helicosphaera waltrans occurs in
the middle part of the Sphenolithus heteromorphus Partial-
range Nannoplankton Zone MNN5, which corresponds to
nannoplankton Zone NN5 of Martini (1971).
Helicosphaera ampliaperta occurs in sediments from
320 m down to 800 m. Therefore, based on the co-occurrence
with S. heteromorphus, this part of Roggendorf-1 can be at-
tributed to the Helicosphaera ampliaperta Zone (nannoplank-
ton Zone NN4). The accompanying taxa are Braaru-
dosphaera bigelowii, Coccolithus pelagicus, Coronocyclus
nitescens, Cyclicargolithus floridanus, Helicosphaera carteri,
H. euphratis, H. scissura, Reticulofenestra daviesii, R. gelida,
R. haqii, R. minuta, Sphenolithus moriformis, Syracosphaera
pulchra, Thoracosphaera spp., Triquetrorhabdulus milowii,
Umbilicosphaera jafarii.
The sediments from 590 m down to 710 m are barren of cal-
careous nannofossils. Most of this interval belongs to the re-
gressive brackish facies of the Rzehakia Beds. In the lower-
most part of the section (samples 790 m and 800 m), very
scarce Sphenolithus belemnos, a marker species of nanno-
plankton Zone NN3, was found. The co-occurring S. hetero-
morphus can be contaminated from the upper part of the sec-
tion. The accompanying assemblage contains Helicosphaera
ampliaperta, H. carteri, H. mediterranea, H. scissura, Cocco-
lithus pelagicus, Coronocyclus nitescens, Cyclicargolithus
floridanus, Reticulofenestra daviesii, R. gelida, R. haqii, R.
minuta, Syracosphaera pulchra, and Thoracosphaera spp.
Foraminifers
The biostratigraphic correlation of the Grund Formation by
means of foraminifers is based primarily on the occurrence of
orbulinas. Orbulina suturalis and Praeorbulina glomerosa
circularis occur together in samples from 210 m. This corre-
sponds to a short interval in the lower part of Middle Mi-
ocene, Langhian, in plankton Zone Mt6, from 15.1 Ma (FAD
of O. suturalis) to around 14.8 Ma (LAD of Po. glomerosa;
comp. Berggren et al. 1995 and Rögl et al. 2002). The com-
mon occurrence of Globorotalia bykovae together with Para-
globorotalia? mayeri seems to be characteristic for the Lower
Badenian. Within the local stratigraphy, uvigerinas are impor-
tant, but rare in the section. Only one specimen of Uvigerina
macrocarinata, the index fossil of the Lower Lagenidae Zone
(Papp & Turnovský 1953), was found, whereas U. grilli oc-
curs rather continuously. The species U. graciliformis defines
the base of the Karpatian, but ranges up into the Lower Bade-
nian Grund Formation.
ROGGENDORF-1, A KEY-SECTION FOR STRATIGRAPHIC POSITION OF GRUND FORMATION 171
Fig. 5. Size variations of Helicosphaera ampliaperta in the sam-
ples 400 m (a) and 800 m (b).
In the Lower Badenian clastic sequence and in the Karpa-
tian Laa Formation, index foraminifers are absent. Planktonic
assemblages are dominated by small Globigerina ottnangien-
sis. The benthic foraminiferal fauna is similarly uncharacteris-
tic in the investigated part of the section (to 410 m).
Helicosphaera ampliaperta taxonomic note
The last occurrence of Helicosphaera ampliaperta is wide-
ly used to define the upper boundary of nannoplankton Zone
NN4 (Martini 1971). This stratigraphically very important
species was described for the first time by Bramlette & Wil-
coxon (1967) from middle Tertiary sediments from the Cipe-
ro section (Trinidad). Originally they described this taxa as
... nearly oval in outline, normally showing little of the termi-
nal flare of the larger (distal) shield, and with no bridge in the
large oval central opening ... and gave a length between 7
and 12 µm. The lower part of the investigated section (740
780 m) contains two clearly different types of this species.
The long axis of the smaller type is about 69 µm (Fig. 5a).
The second type encompasses specimens, whose long axis is
larger than 10 µm (Fig. 5b). This type occurs in the whole part
of the section identified as the NN4 Zone. Our investigation
shows that these two size-defined types can be very useful for
the stratigraphy of Lower Miocene sediments.
Conclusions
The lowermost investigated part (Robulus Schlier) con-
taining Sphenolithus belemnos a marker of nannoplankton
Zone NN3 is correlated to nannoplankton Zone NN3/4 by
the co-occurrence of S. heteromorphus. The microflora is in-
dicative for more eutrophic conditions (Fig. 4c). The upper-
most part of the Robulus Schlier consists of layered, partly
non-calcareous shales and fine sands with fish remains. This
shows some similarities with fish shales of the Zellerndorf
Formation (Ottnangian), and with non-calcareous parts of the
so-called Robulus Schlier south of the Danube (e.g. in
prospection drill site NÖ-03, Schaubing). The nannoplankton
indicates a biostratigraphic position within nannoplankton
Zone NN4. During the Late Ottnangian, paleoecological con-
ditions were intermediate between eutrophic and oligotrophic
conditions (Fig. 4b,c).
The sandy sedimentation of the Rzehakia Beds is barren of
nannofossils and foraminifers. The lower boundary is based
on the lithology and additionally up-section by the appearance
of a new foraminiferal assemblage at 678 m. A similar se-
quence was observed in the Goggendorf U1 drill site (Cicha
1999b).
The Karpatian Laa Formation (360612 m) is correlated to
nannoplankton Zone NN4, but the assemblages of the hang-
ing wall and the underlying Ottnangian are distinctly different
(Fig. 2, Appendix A). The basal samples are barren. There-
fore, the lower boundary is based on a change in lithology at
612 m. Benthic assemblages point to a deepening upward and
partly dysoxic bottom conditions. The nannoflora, with an in-
crease of C. pelagicus of more than 90 %, the interpretation of
the nMDS plots (Fig. 4ac) and small globigerinas indicate
cooler surface water, upwelling conditions and increasing nu-
trient supply. The 250 m of Karpatian sediments in Roggen-
dorf-1 represent only a small part of the normal thickness in
the Molasse Basin, e.g. about 1000 m of incomplete thickness
in the water drill site Laa Thermal Süd 1. There, poor plank-
tonic foraminiferal assemblages and pyritized diatoms simi-
larly characterize the lower part of the Laa Formation, show-
ing an up-section increase of agglutinated foraminifers (Cicha
1997).
Within the clastic sequence (270347 m) a biostratigraphic
dating as Badenian was possible based on nannoplankton
only. The boundary between nannoplankton Zones NN4 and
NN5 was observed at 320 m. In the Styrian Basin, nanno-
plankton Zone NN4 was documented in the Lower Badenian
also (Rögl et al. 2002). The basal gravels (347360 m) are re-
garded as the transgressive base of the Badenian in the Molas-
se Basin north of the Danube. In the interval from 350 m to
270 m a stepwise decrease of the Cp/Rm % value from 80 %
to 10 %, as well as the nMDS plot, demonstrate a gradual
change to warmer conditions accompanying the transition
from the Laa to the Grund Formations.
The fine clastic sediments of the Grund Formation (2
255 m) belong to nannoplankton Zone NN5, and are dated at
the top by planktonic foraminifers as the lower part of plank-
ton Zone Mt6 (Orbulina suturalis/Globorotalia peripher-
oronda Concurrent Range Zone of Berggren et al. 1995). The
level with G. bykovae and P. mayeri, recorded in the lower
part of the Grund Formation in Roggendorf-1, corresponds to
the lower part of the Grund Formation in Cicha (1999a) and
vábenická & Ètyroká (1999), attributed there to the Karpa-
tian. Paleoecologically, the Grund Formation in Roggendorf-1
shows a deepening upward sequence to water depths of the
outer shelf. The surface waters were warm, as indicated by the
low percentages of Coccolithus pelagicus (low value of Cp/
Rm %, Fig. 2) and a relatively high number of the planktonic
foraminifer Globigerinoides. This is clearly expressed by the
nMDS plots (Fig. 4ac). The conglomerates at 255270 m are
considered to be the coarse basal transgression level of the
Grund Formation because the nannoplankton paleoecology is
in good agreement with the overlying fine clastics (Fig. 2).
172 ÆORIÆ and RÖGL
Acknowledgments: This study is part of FWF Project P-13743-
BIO (Austrian Science Fund, project leader J. Hohenegger),
which was made possible by the OMV AG, Vienna, which
provided samples and bore hole logs. For discussion and in-
formation we are grateful to B. Krainer and R. Peschel (OMV
AG, Vienna), J. Hohenegger (University of Vienna), and to R.
Roetzel (Geological Survey, Vienna). For technical assistance
we thank T. Suttner. The text was kindly rewieved by: R.
Brzobohatý (Brno), I. Magyar (Budapest), T. Peryt (Warsza-
wa) and F.F. Steininger (Frankfurt a.M.).
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ROGGENDO
RF-1,
A
K
EY-SECTION
FOR
STRATIGRAPHIC
POSITION
OF
GRUND
FORMATION
173
Appendix A: Distribution of calcareous nannoplankton in the borehole Roggendorf-1.
174 ÆORIÆ and RÖGL
Appendix B/1
ROGGENDORF-1
Foraminifers
27
m
7
10 m
130 m
150 m
160 m
170 m
180 m
210 m
220 m
240 m
260 m
270 m
280 m
285 m
290 m
295 m
300 m
320 m
330 m
350 m
370 m
380 m
390 m
400 m
410 m
Bathysiphon filiformis M. Sars
x x
Budashevaella wilsoni (Smith)
x
Haplophragmoides vasiceki vasiceki Cicha et Zapl.
x x x
Karrerotextularia sp.
x
x
Martinotiella communis (dOrbigny)
x x x x x x
Martinotiella karreri (Cushman)
x
x x
Semivulvulina deperdita (dOrbigny)
x x x x
Siphotextularia concava (Karrer)
x x x
Siphotextularia sp.
x
Spirorutilus carinatus (dOrbig+A45 ny)
x x x x
x
Textularia laevigata dOrbigny
x x x x
Textularia mariae dOrbigny
x
Cycloforina sp.
x
x
Lachlanella incrassata (Karrer)
x
Nodobaculariella sp.
x
Pyrgo simplex (dOrbigny)
x
Quinqueloculina akneriana dOrbigny
x
Quinqueloculina buchiana dOrbigny
x x
x x x
Quinqueloculina seminulina (Linné)
x
Sigmoilinita tenuis (Czjzek)
x x x x x x
Sigmoilopsis celata (Costa)
x x x x
x
Sinuloculina cyclostoma (Reuss)
x
Spiroloculina excavata dOrbigny
x x x
Spirillina vivipara Ehrenberg
x
Alabamina armellae Popescu
x
Ammonia pseudobeccarii (Putrja)
x
x x x x x x x
x x x
Ammonia tepida (Cushman)
x x x
Ammonia viennensis (dOrbigny)
x x x
x x
x x
x
x
Amphicoryna badenensis (dOrbigny)
x x x x x x x x x
Amphicoryna hispida (d'Orbigny)
x x x x
x
Amphimorphina haueriana Neugeboren
x x x x x x
x x
Angulogerina angulosa (Williamson)
x x x x x x x x
x
Asterigerinata mamilla (Williamson)
x
Asterigerinata planorbis (dOrbigny)
x x x x
Aubignyna brixi Rögl
x
x
Aubignyna sp.
x x
Biapertorbis biaperturata Pokorný
x
Bolivina antiqua dOrbigny
x
x
Bolivina antiquaeformis Cicha et Zapletalová
x
Bolivina dilatata brevis Cicha et Zapletalová
x x x
x
x
Bolivina dilatata dilatata Reuss
x x x x x x x
x
x x x
Bolivina hebes Macfadyen
x x x x x x x
x x
x x
Bolivina aff. iriensis Tedeschi
x
Bolivina cf. lowmani Phleger et Parker
x x
Bolivina plicatella Cushman
x x x x
Bolivina pokornyi Cicha et Zapletalová
x
Bolivina pseudoplicata Heron-Allen et Earland
x
Bolivina scalprata retiformis Cushman
x x x x
Bolivina sp. (aff. simplex Phleg. et Park. acc. C.&Z.)
x x x x x
x
x x
Buccella granulata (Di Napoli)
x
Bulimina buchiana dOrbigny
x x x
Bulimina striata mexicana Cushman
x x x x x x
x
Bulimina striata striata dOrbigny
x x x x x x x x
Buliminella elegantissima dOrbigny
x
Cassidulina carinata Silvestri
x
x
x x
Cassidulina laevigata dOrbigny
x x x
Cassidulina margareta Karrer
x x
x x
Appendix B: Distribution of benthic and planktonic foraminifers in the borehole Roggendorf-1.
Appendix B/1
ROGGENDORF-1, A KEY-SECTION FOR STRATIGRAPHIC POSITION OF GRUND FORMATION 175
Appendix B/2
ROGGENDORF-1
Foraminifers
27 m
710 m
130 m
150 m
160 m
170 m
180 m
210 m
220 m
240 m
260 m
270 m
280 m
285 m
290 m
295 m
300 m
320 m
330 m
350m
370 m
380 m
390 m
400 m
410 m
Caucasina cylindrica Zapletalová
x
x
x
Caucasina elongata (dOrbigny)
x x x
Caucasina schischkinskayae Samoylova
x x x
x x x
x
x
Caucasina subulata (Cushman et Parker)
x x x x x x x
x x
x x
Ceratobulimina contraria (Reuss)
x
Ceratocancris haueri (dOrbigny)
x
x x
x x
Chilostomella ovoidea Reuss
x
Cibicides refulgens Montfort
x
Cibicidoides spp.
x
x x x x x x x
x x
x
x
Cibicidoides lopjanicus (Myatlyuk)
x
x
x
x
Cibicidoides ungerianus (dOrbigny)
x x x x x x
Dentalina beyrichana Neugeboren
x
Dimorphina akneriana (Neugeboren)
x x
Discorbinoides patelliformis (Brady)
x
Elphidiella dollfusi (Cushman)
x
Elphidiella subnodosa (Reuss)
x
Elphidium cf. angulatum (Egger)
x x
x
Elphidium flexuosum (d'Orbigny)
x
x
Elphidium praeforme Papp
x
Elphidium reussi Marks
x
Elphidium ungeri (Reuss)
x
Eponides pusillus Parr
x x x x x
x
Favulina hexagona (Williamson)
x
Fissurina aperta Seguenza
x
Fissurina solida Seguenza
x
Fissurina? aequabilis (Matthes)
x
Fursenkoina acuta (dOrbigny)
x x
x
Gavelinopsis praegeri (Heron-Allen et Earland) x
Glabratellina sp.
x
Glandulina laevigata d'Orbigny
x
Globocassidulina oblonga (Reuss)
x x
x
x
Globocassidulina subglobosa (Brady)
x x
x x
x
x
x
Globobulimina pupoides (dOrbigny) s.l.
x
x
x
x
Globobulimina pyrula (dOrbigny)
x
Globulina gibba dOrbigny
x
x
Globulina punctata dOrbigny
x
Grigelis? mariae (dOrbigny)
x x
Guttulina austriaca dOrbigny
x
x x x
Guttulina communis dOrbigny
x
Gyroidinoides octocameratus (Cushman)
x x x x x
x
x
x
Gyroidinoides soldanii (dOrbigny)
x x x x
x
Gyroidinoides umbonatus (Silvestri)
x x x x x
x x
x
Hanzawaia boueana (dOrbigny)
x
x
x
Hemirobulina glabra (dOrbigny)
x
x
Hemirobulina spp.
x
x
x
Heterolepa praecincta (Karrer)
x x x
x x x x
x
x
Heterolepa dutemplei (dOrbigny)
x
x
x x
Hoeglundina elegans (dOrbigny)
x x x x x
x
Hyalinonetrion elongatum (Ehrenberg)
x
Laevidentalina badenensis (dOrbigny)
x
Laevidentalina spp.
x
Lagena haidingeri (Czjzek)
x
x
Lagnea sp.
x
Lapugyina schmidi Popescu
x x x x x
x
Lenticulina americana (Cushman)
x x
x
Lenticulina austriaca (dOrbigny)
x x x x x
x
x
Lenticulina calcar (Linné)
x
Appendix B/2
176 ÆORIÆ and RÖGL
Appendix B/3
ROGGENDORF-1
Foraminifers
27
m
7
10 m
130 m
150 m
160 m
170 m
180 m
210 m
220 m
240 m
260 m
270 m
280 m
285 m
290 m
295 m
300 m
320 m
330 m
350 m
370 m
380 m
390 m
400 m
410 m
Lenticulina inornata (dOrbigny)
x x x
Lenticulina melvilli (Cushman et Renz)
x
Lenticulina orbicularis (dOrbigny)
x
x
Lenticulina spinosa (Cushman)
x
Lenticulina spp.
x x x x x x x x x
x
Lobatula lobatula (Walker et Jacob)
x x x
Marginulina hirsuta dOrbigny
x
Melonis pompilioides (Fichtel et Moll)
x x x x x
x x
Myllostomella advena (Cushman et Laiming)
x x x x x x x x
x
x
x x x
Myllostomella recta (Palmer et Bermudez)
x x
x x
x
Neoconorbina terquemi (Rzehak)
x
Neugeborina irregularis (dOrbigny)
x x
Neugeborina longiscata (dOrbigny)
x x
x
Nonion commune (dOrbigny)
x x x x x x x x x
x
x
Nonionella turgida (Williamson)
x
x
Nonionoides? exesa (Langer)
x x
Nonionoides karaganicus (Krasheninnikov)
x x x x x
x
Nonionoides ventragranosus (Krasheninnikov)
x
Nuttallides convexus (Parker)
x x
Oridorsalis umbonatus (Reuss)
x x x x
Orthomorphina ambigua (Neugeboren)
x
Orthomorphina sp.
x x
Pappina primiformis (Papp et Turnovský)
x
Pappina breviformis (Papp et Turnovský)
x x
x
Planularia moravica (Karrer)
x
Plectofrondicularia digitalis (Neugeboren)
x
Plectofrondicularia medelingensis (Karrer)
x x
Porosononion granosum (dOrbigny)
x
x
x
Pseudoparrella exigua (Brady)
x x
x
x
x
x
Pseudosolenia lateralis carinata (Buchner)
x
Pullenia bulloides (dOrbigny)
x x x x x x x x
x x
Pullenia quinqueloba (Reuss)
x
Reussella laevigata Cushman
x
x
Siphonodosaria consobrina (dOrbigny)
x
x x
x
Siphonodosaria nuttalli gracillima (Cush. et Jarvis) x x x x
Siphonodosaria scabra (Reuss)
x x
x
Siphonodosaria scripta (dOrbigny)
x
Sphaeroidina bulloides dOrbigny
x x x
x
x
Spiroloxostoma czechoviczi (Kantorova)
x x
Stilostomella adolphina (dOrbigny)
x x x x x
Stilostomella? sp.
x
Trochulina patella (Reuss)
x
Uvigerina acuminata Hosius
x
x
x
Uvigerina graciliformis Papp et Turnovský
x x x
x
Uvigerina grilli Schmid
x cf. x x
x
Uvigerina cf. laviculata Coryell et Rivero
x
Uvigerina macrocarinata Papp et Turnovský
cf.
Uvigerina saprophila Daniels et Spiegler
x
x
Uvigerina semiornata d'Orbigny
x x
x x
Valvulineria complanata (dOrbigny)
x x x x x x x x x
x
x
x x x
Valvulineria? minuta (Schubert)
x
Virgulopsis tuberculatus (Egger)
x x
Appendix B/3
ROGGENDORF-1, A KEY-SECTION FOR STRATIGRAPHIC POSITION OF GRUND FORMATION 177
Appendix B/4
ROGGENDORF-1
Foraminifers
27
m
71
0m
130
m
150
m
160
m
170
m
180
m
210
m
220
m
240
m
260
m
270
m
280
m
285
m
290
m
295
m
300
m
320
m
330
m
350
m
370
m
380
m
390
m
400
m
410
m
Globigerina cf. bollii Cita et Premoli-Silva
x x x
x
x
Globigerina bulloides dOrbigny
x x x x x x x
x x
x
Globigerina concinna Reuss
x x x
x
x
Globigerina diplostoma Reuss
x x x x
Globigerina dubia Egger
x
Globigerina cf. falconensis Blow
x x
x x x x x
Globigerina ottnangiensis Rögl
x x x x
x x
x x x x
x x x x x
Globigerina praebulloides Blow
x x x x x x x x x
x x
x
x x
Globigerina tarchanensis Subbotina et Chutzieva
x
x x
x x
x x
Globigerinella regularis (dOrbigny)
x x x x x x x
Globigerinoides bisphericus Todd
x x
Globigerinoides quadrilobatus (dOrbigny)
x x x x x x x
x
Globigerinoides trilobus (Reuss)
x x x x x
Orbulina suturalis Brönnimann
x x
Praeorbulina glomerosa circularis (Blow)
x x
Globoturborotalita connecta (Jenkins)
x
Globoturborotalita druryi (Akers)
x x x
x
Globoquadrina cf. altispira (Cushman et Jarvis)
x
x
Globorotalia bykovae (Aisenstadt)
x x x x x x x x x x
Paragloborotalia? acrostoma (Wezel)
x
x
x
Paragloborotalia? cf. continuosa (Blow)
x x x
x
Paragloborotalia? inaequiconica (Subbotina)
x x x x x
x
x
Paragloborotalia? mayeri (Cushman et Ellisor)
x x x x x x
x x
Globigerinita glutinata (Egger)
x x x x x x x x
x
x
x x
Globigerinita uvula (Ehrenberg)
x x x x x x x x x
Tenuitella cf. clemenciae (Bermudez)
x
x x
Tenuitellinata angustiumbilicata (Bolli)
x
x x
x
x
x x
Tenuitellinata selleyi Li, Radford et Banner
x x x x
x
x x
x x
x
x x x x x
Turborotalita neominutissima (Bermudez et Bolli)
x
x x x x
x
x x
x
x
Turborotalita quinqueloba (Natland)
x x x x x x x
x
x x x x
x
x x x x x
Turborotalita sp. 1
x x
x x
x
Turborotalita sp. 2 (clarkei-group)
x x
Cassigerinella globulosa (Egger)
x
x
Cassigerinella spinata Rögl
x x
Cassigerinella boudecensis Pokorný
x x x x x x x x x x
x
x
Appendix B/4
178 ÆORIÆ and RÖGL
Appendix C: Bray-Curtis Similarity of calcareous nannofossils; dissimilarity values are available upon request (C pel Cocco-
lithus pelagicus, Hel am Helicosphaera ampliaperta, Hel sc Helicosphaera scissura, Ret ha Reticulofenestra haqii, Ret min
Reticulofenestra minuta, Sy pu Syracosphaera pulchra).
Group 1
Average similarity: 66.67
Species
Av.Abund
Av.Sim
Sim/SD
Contrib%
Cum.%
C pel
15.00
57.14
#######
85.71
85.71
Ret min
2.00
4.76
#######
7.14
92.86
Group 2
Average similarity: 89.46
Species
Av.Abund
Av.Sim
Sim/SD
Contrib%
Cum.%
Ret min
316.60
81.91
13.94
91.56
91.56
Group 3
Average similarity: 82.89
Species
Av.Abund
Av.Sim
Sim/SD
Contrib%
Cum.%
Ret min
197.50
57.49
10.70
69.35
69.35
C pel
76.17
22.06
6.16
26.61
95.97
Group 4
Average similarity: 68.66
Species
Av.Abund
Av.Sim
Sim/SD
Contrib%
Cum.%
C pel
123.86
32.51
3.92
47.35
47.35
Ret min
57.43
13.53
2.70
19.71
67.06
Sy pu
48.71
12.82
7.12
18.67
85.73
Ret ha
41.43
5.20
0.87
7.58
93.31
Group 5
Average similarity: 61.82
Species
Av.Abund
Av.Sim
Sim/SD
Contrib%
Cum.%
C pel
129.60
38.86
3.80
62.87
62.87
Hel am
21.40
6.41
2.48
10.38
73.24
Sy pu
19.00
5.64
1.36
9.13
82.37
Hel sc
9.60
2.77
4.21
4.47
86.84
Ret ha
6.40
2.28
5.22
3.68
90.53
Group 6
Average similarity: 56.96
Species
Av.Abund
Av.Sim
Sim/SD
Contrib%
Cum.%
C pel
150.50
49.90
#######
87.59
87.59
Sy pu
29.00
5.41
#######
9.49
97.08