GEOLOGICA CARPATHICA, 53, 3, BRATISLAVA, JUNE 2002
197 — 210
CALCAREOUS NANNOFOSSILS OF THE UPPER KARPATIAN AND
LOWER BADENIAN DEPOSITS IN THE CARPATHIAN FOREDEEP,
MORAVIA (CZECH REPUBLIC)
LILIAN ŠVÁBENICKÁ
Czech Geological Survey, Klárov 131/3, 118 21 Prague, Czech Republic; svab@cgu.cz
(Manuscript received November 13, 2001; accepted in revised form March 19, 2002)
Abstract: Calcareous nannofossils were studied in the Karpatian and Lower Badenian deposits of the Carpathian Foredeep,
Moravia in view of their use in biostratigraphy. The following nannofossil horizons were recognized: 1. “helicolith”
horizon with common Helicosphaera ampliaperta in sandy clays (“schlier”) of the Laa Formation, 2. Helicosphaera
waltrans horizon in clays and siliciclastic sediments of the Grund Formation and in the basal siliciclastic sediments of the
Lower Badenian, and 3. Sphenolithus heteromorphus horizon in clays (“tegel”) of Lower Badenian (Moravian) age. In
its upper part, oval forms of Coronocyclus nitescens and 5-rayed symmetrical discoasters appear. The occurrence of
species H. waltrans is limited to a short stratigraphic interval approximately corresponding to the range of planktonic
foraminiferal species Globigerinoides bisphericus and includes the first appearances of Praeorbulina ssp. and Orbulina
suturalis. The dominance of helicoliths in the Laa and Grund formations and in the basal siliciclastic sediments of the
Lower Badenian gives evidence for a shallow epicontinental sea. Nannofossil enrichment above the Helicosphaera
waltrans horizon evidences deepening of depositional area, open-sea conditions, and reflects the Lower Badenian trans-
gression. The problem of correlation of the Central Paratethys regional stages either with the Mediterranean
chronostratigraphic scale or with NN zones was discussed.
Key words: Carpathian Foredeep, Miocene, Karpatian, Badenian, calcareous nannofossils, biostratigraphy, paleoecology.
Introduction
The Carpathian Foredeep is a foreland basin bordering the
West-Carpathian arch along its distal periphery. Paleogeo-
graphically, it is included into the intercontinental basins of
the Central Paratethys. In the Oligocene and Miocene, this
area was a region of shallow, variable-salinity basins with
specific macrofauna, microfauna and nannoflora. The com-
plicated paleogeographical development of the Central Parat-
ethys influenced mainly by the terminal phases of the Alpine
Orogeny has been broadly studied, recently by Rögl (1998),
Kováč et al. (1998), Jarosiński & Krzywiec (2001) and oth-
ers.
Biostratigraphic evaluation based on calcareous nannofos-
sils was carried out for the Lower to Middle Miocene deposits
of the Carpathian Foredeep, southern and central Moravia,
Czech Republic (Fig. 1). Attention was focused on the Karpa-
tian-Badenian strata where foraminifers with species Globi-
gerinoides bisphericus and genera Praeorbulina and Orbulina
appear for the first time, and on the overlying Lower Badenian
deposits.
Nannofossil species Helicosphaera waltrans was found to
be a significant marker for biostratigraphic subdivision of the
Karpatian and Badenian sediments within the NN4/NN5 zone
boundary. Its occurrence forms a significant interval with
probably short stratigraphic range.
The aim of the present study was to analyse nannofossil as-
semblage with H. waltrans and the assemblages below and
above the occurrences of this species and to test the eligibility
of H. waltrans as a zonal marker in the Carpathian Foredeep.
Previous studies
Biostratigraphic evaluation of the Karpatian and Badenian
deposits of the Carpathian Foredeep in Moravia was largely
based on foraminifers, especially in the papers by Vašíček
(1949) and Molčíková (1967). Attention was focused on Kar-
patian foraminifers by Cicha & Zapletalová (1967) and Papp
et al. (1978). Modern biostratigraphic interpretations are pre-
sented in the works of Cicha (1995, 1999, 2001), Cicha et al.
(1998), Pálenský & Čtyroká (1994), Cicha & Čtyroká (1995),
Čtyroká et al. (1995) and Čtyroká & Pálenský (1997).
Calcareous nannofossils were studied by Molčíková (1974,
1978, 1983). She distinguished the Karpatian Stage from the
Badenian one within zone NN5, according to the first occur-
rence of the species Discoaster variabilis. Lehotayová &
Molčíková (1978) presented an overview on Badenian nanno-
fossil assemblages in the territory of former Czechoslovakia.
The first comparisons of nannofossil biostratigraphy with fora-
miniferal data have been carried out by Čtyroká & Švábenická
(1997, 2000) and Švábenická & Čtyroká (1998, 1999).
In the Polish part of the Carpathian Foredeep, Middle Mi-
ocene nannofossils were described by Martini (1977), Gonera
& Slezak (in Cieszkowski et al. 1988) and Dudziak & Łaptaś
(1991). In the Outer Western Carpathians, Slezak et al. (1995)
attributed the terminal flysch deposits of the Skole Nappe to
the early Lower Badenian, zone NN5. The correlation of nan-
nofossils with foraminiferal microfauna in the Polish part of
Central Paratethys was presented by Dudziak & Łuczkowska
(1991) and in the Outer Carpathians and its foredeep by Garec-
ka & Olszewska (1998).
198 ŠVÁBENICKÁ
Fig. 1. Schematic geological map of the western part of the Western Carpathians, and the location of the study area.
Fig. 2. A sketch map of the Carpathian Foredeep, southern and central Moravia, Czech Republic, showing the location of the studied lo-
calities and major cities (in capitals). Nannofossil horizons are marked in colours.
CALCAREOUS NANNOFOSSILS OF THE KARPATHIAN AND BADENIAN DEPOSITS 199
Nannofossil associations from the lower part of the Bade-
nian were described by Lehotayová (1975) in the Danube
Lowland. A comparison of the Karpatian nannofossil assem-
blages (zones NN4 and NN5) in the Intra-Carpathian basins of
Slovakia with those of the same age from the Carpathian Fore-
deep in Moravia was worked out by Lehotayová (1984). The
nannoplankton biostratigraphy of the Lower and Middle Mi-
ocene deposits of the Vienna Basin, Slovak Republic and its
comparison with the Mediterranean and Paratethyan zonations
was presented by Andreyeva-Grigorovich et al. (2001). In this
paper, the short stratigraphic range of Helicosphaera waltrans
is correlated within the midle part of Badenian.
Fuchs & Stradner (1977) combined foraminiferal and nanno-
fossil data in the study of Badenian sediments of the Vienna
Basin, Austria. Nannofossil assemblages of zone NN5 with
Sphenolithus heteromorphus and discoasters were correlated
with the “Untere Lageniden-Zone” where planktonic foramini-
fers Globigerinoides bisphericus and Praeorbulina glomerosa
s.l. appear for the first time. Stradner & Fuchs (1978) presented
an overview of nannoplankton in the Badenian strata (zones
NN5 and NN6/7) of Austria. Švábenická (1993, 2000) focused
on the species Helicosphaera waltrans as a significant marker
in the Karpatian-Badenian boundary strata of the Alpine-Car-
pathian Foredeep, Lower Austria.
Lower and Middle Miocene nannofossils in the Hungarian
territory of the Paratethys were broadly studied by Báldi-Beke
& Nagymarosy (1979), Báldi-Beke (1980, 1982) and Nagy-
marosy (1985). In Romania, Mărun eanu (1992, 1993, 1999)
reported the occurrence of index nannofossil species in the
Miocene deposits of Intra- and Extra-Carpathian basins, and
compared it with the Mediterranean and Paratethyan areas.
The Karpatian/Badenian boundary is placed here within the
Langhian Stage of the general stratigraphic classification.
As concerns the Eastern Paratethys, Andreyeva-Grigoro-
vich & Savytskaya (2000) worked out a nannofossil stratigra-
phy within zone NN5 (Tarkhanian/Langhian) and correlated it
with the Central Paratethys and Mediterranean stages.
Material
Calcareous nannofossils were studied from the Lower-Mid-
dle Miocene boundary deposits of Carpathian Foredeep in the
area of southern and central Moravia, Czech Republic (Fig. 2).
Fig. 3. Carpathian Foredeep, southern and central Moravia, Czech Republic. Distribution of calcareous nannofossil taxa the first occurrence
of which is mostly known in the Miocene. Abundance of nannofossil taxa: C – common (>1 specimen per field of view), F – few (1—10
specimens per 10 fields of view), R – rare (1—10 specimens per 20 fields of view), VR – very rare (<1 specimen per 20 fields of view).
Preservation of nannofossils: M – moderate (etching or mechanical damage is apparent but majority of specimens are easily identifiable),
P– poor (etching and especially mechanical damage is intensive making identification of some specimens difficult). Estimates of the abun-
dance of nannofossils in samples: VH = very high (>20 specimens per field of view), H – high (10—20 specimens per field of view), M –
moderate (5—10 specimens per field of view), L – low (1—5 specimens per field of view), VL – very low (<1 specimen per field of view).
Localities
Sample No.
preservation of nannofossils
abundance of nannofossils
% of reworked specimens (estimate)
Braarudosphaera bigelowii
Calcidiscus leptoporus
Calcidiscus macintyrei
Calcidiscus premacintyrei
?
Catinaster
sp.
Coccolithus miopelagicus
Coronocyclus nitescens
(circular forms)
Coronocyclus nitescens
(oval forms)
Discoaster adamanteus
Discoaster deflandrei
Discoaster exilis
Discoaster variabilis
Discoaster
sp.
(5-rayed forms)
Helicosphaera ampliaperta
Helicosphaera carteri
Helicosphaera mediterranea
Helicosphaera scissura
Helicosphaera vedderi
Helicosphaera walbersdorfensis
Helicosphaera waltrans
Pontosphaera discopora
Pontosphaera multipora
Reticulofenestra haqii
Reticulofenestra minuta
Reticulofenestra pseudoumbilicus
(<7
µ
m
Reticulofenestra pseudoumbilicus
(>7
µ
m)
Rhabdosphaera sicca
Rhabdosphaera
sp.
Sphenolithus heteromorphus
Syracosphaera
sp.
Triquetrorhabdulus
sp.
Umbilicosphaera rotula
A
M
L
98
R
VR
VR
R
R
B
M
L
98
R
R
R
VR
VR
1
P
M
98
R
VR
R
VR
VR VR
?
VR
2
M
M
95
R
F
VR
F
VR
VR
Žopy
224
P
VL 90
VR
F
VR
VR
VR VR
301 m
P
L
90
C
VR
R
287 m
P
L
90
VR
VR
VR
VR
R
F
VR
R
VR
R
R
F
VR
VR VR
238 m
M VH 75
VR
R
VR
F
VR
R
VR VR
C
F
F
F
C
F
R
F
F
R
210 m
M
L
80
R
VR
VR
R
C
VR VR
F
R
R
R
F
VR
VR
1
P
L
95
R
R
VR
VR
VR VR
R
VR
VR
3
P
L
95
R
VR
R
R
VR
R
VR
R
VR
6
P
L
99
VR
VR
VR
VR
7
M
M
95
VR
VR
R
VR
VR
R
F
R
R
VR
8
P
L
99
VR
VR
VR VR
VR
VR VR VR
VR
9
P
L
95
VR
F
VR
F
VR VR VR
R
R
P
L
95
VR
VR
F
R
F
VR
R
R
Hradčany
14
M VH 90
?
R
VR
VR VR
R
F
VR
F
R
R
R
R
VR
VR
R
Kelčice
K1
M
H
90
VR
R
VR
R
VR
F
R
VR
F
VR
R
R
R
R
R
Veselíčko
31
M
H
85
R
R
R
VR
VR
R
R
VR
VR
F
VR
R
R
VR
R
R
VR
R
R
VR
4
M VH 60
R
R
F
VR
F
F
VR
R
F
R
R
R
R
R
F
R
23
M
M
90
VR
R
VR
R
VR
R
R
R
VR
VR VR
R
R
R
Slatinice
A
M
H
75
R
R
R
R
F
VR
F
VR
R
R
R
VR
R
R
C
R
5
M
M
40
R
F
C
C
F
R
R
R
F
R
R
C
R
F
6
M
H
50
R
R
R
C
C
VR
F
F
R
F
F
F
C
F
R
R
F
7
M
H
60
?
F
R
C
C
F
F
F
F
R
C
C
R
VR
R
8
M
H
50
R
F
?
F
R
F
C
C
R
C
F
C
R
F
C
C
F
R
R
F
9
M
H
50
F
F
F
F
R
C
C
F
F
R
F
R
C
F
F
F
F
C
S2
M
M
30
R
F
F
R
C
C
VR
C
VR
F
F
R
F
C
F
F
R
Vsisko
6
M VH 70
?
C
F
C
C
C
R
F
F
F
C
F
F
Hejčín
H1
M VH 90
C
R
R
VR
C
VR
F
R
R
R
F
F
R
2
M VH 80
R
R
R
R
C
C
F
VR
R
F
F
R
F
C
F
3
M
M
80
VR
R
VR
C
VR
R
F
R
R
F
C
K2
M
M
60
R
R
R
R
F
R
R
F
C
R
F
R
C
C
F
R
R
R
F
2
M
H
50
R
F
C
F
C
F
F
F
F
F
F
C
F
F
F
C
Kuřim-Pod Jánečkem
M
H
60
R
R
F
C
R
R
C
C
R
C
F
F
F
F
F
F
F
C
Kuřim
V101
M VH 40
F
?
C
R
R
C
C
R
VR
C
F
C
F
F
C
C
F
R
F
F
Slavonín
Neředín
Křelov
Novosedly
Hrušovany n. J.
Šatov
Velký Týnec
Opatovice
HJ-103
Troskotovice
200 ŠVÁBENICKÁ
The deposits comprise Karpatian sandy clays (“schlier”) of the
Laa Formation and Karpatian-Badenian siliciclastic sediments
and clays of the Grund Formation (sensu Cicha 2001). Above,
Lower Badenian basal and marginal siliciclastic sediments,
clays (“tegel”) and Lithothamnion Limestone were deposited.
Lower Badenian clays (“tegel”) are characterized by the pres-
ence of benthic Lanzendorf microfauna (Cicha & Tejkal
1965).
Material was sampled during mapping and other geological
works. This contribution gives an overview of all available
data. The results are considered to be state-of-the-art. Precise
correlation remains obscure because no continuous section
crossing the Karpatian/Badenian boundary and overlying
Lower Badenian strata has been made yet.
Methods
Suspension slides were prepared using a decantation method
(separated fraction of 3—30 µm in the following procedure: the
heavy fraction was allowed to settle for 3 minutes in a 45-mm
water column, the fine fraction for 45 minutes). Slides were
inspected with a Nikon light-microscope at 1000
×
magnifica-
tion.
Quantitative data on Miocene taxa mentioned in this study
were obtained by counting the number of specimens per field
of view under the microscope. This method was chosen be-
cause of the presence of a high number of reworked nannofos-
sils in taphocoenoses.
Biostratigraphic conclusions were based exclusively on spe-
cies whose first appearance is known from the Miocene. Bios-
tratigraphic data were compared with the standard nanno-
plankton NN zones of Martini (1971) and Young (1998), and
MNN (Mediterranean Neogene Nannoplankton) zones of For-
naciari et al. (1996).
Results
Samples provided moderately well or poorly preserved cal-
careous nannofossils (Fig. 3). Large placoliths and helicoliths
(>10 µm in long axis) occur mostly in fragments and the distal
rays of discoasters are broken or strongly etched especially in
deposits with an admixture of sand and silt.
Fig. 4. Carpathian Foredeep, southern and central Moravia, Czech Republic. Distribution of stratigraphically significant calcareous nan-
nofossils in the Karpatian and Lower Badenian deposits and delimination of nannoplankton horizons.
Fig. 5. Miocene calcareous nannofossils of the Karpatian and Lower Badenian deposits in the Carpathian Foredeep, Moravia (Czech Republic).
PPL – plane-polarized light, XPL – cross-polarized light. 1—6 – Helicosphaera carteri (Wallich) Kamptner. 1, 2 – Lower Badenian clays,
Vsisko No. 71; 1: PPL, 2: XPL; 3, 4 – Lower Badenian clays, Hejčín No. 28; 3: PPL, 4: XPL; 5, 6 – Laa Formation, Novosedly No. 2; 5: PPL,
6: XPL. 7—12 – Helicosphaera ampliaperta Bramlette et Wilcoxon, Laa Formation. 7, 8 – Novosedly No. 2; 7: PPL, 8: XPL; 9—12 – Opato-
vice HJ103 (301.7 m); 9,11: PPL, 10,12: XPL. 13—16 – Helicosphaera mediterranea Müller, Laa Formation. 13, 14 – Hrušovany; 13: PPL,
14: XPL; 15, 16 – Novosedly No. 2; 15: PPL, 16: XPL. 17—30 – Helicosphaera waltrans Theodoridis. 17—20 – basal siliciclastic sediments
of the Lower Badenian, Hradčany No. 14/1; 17,19: PPL, 18,20: XPL; 21—24 – Grund Formation, Šatov No. 7; 21,23: PPL, 22,24: XPL; 25—28
– Grund Formation, Opatovice HJ103 (210.6 m); 25,27: PPL, 26,28: XPL; 29, 30 – basal siliciclastic sediments of the Lower Badenian,
Kelčice No. K1; 29: PPL, 30: XPL. 31—36 – Helicosphaera walbersdorfensis (Müller) Theodoridis, Lower Badenian clays. 31,32: Slatinice
No. A; 31: PPL, 32: XPL; 33—36 – Velký Týnec No. 75; 33,35: PPL, 34,36: XPL. Reworked nannofossil specimens (helicoliths) from the
Eocene and Oligocene sediments. 37—38 – Helicosphaera compacta Bramlette et Wilcoxon, Lower Badenian clays. Vsisko No. 71; 37: PPL,
38: XPL. 39—40 – Helicosphaera recta (Haq) Jafar et Martini, Lower Badenian clays. Vsisko No. 71; 39: PPL, 40: XPL. 41—42 – Heli-
cosphaera intermedia Martini, Lower Badenian clays. Hejčín No. 28; 41: PPL, 42: XPL. Microphotographs by L. Švábenická.
▲
CALCAREOUS NANNOFOSSILS OF THE KARPATHIAN AND BADENIAN DEPOSITS 201
202 ŠVÁBENICKÁ
CALCAREOUS NANNOFOSSILS OF THE KARPATHIAN AND BADENIAN DEPOSITS 203
Three horizons of calcareous nannofossils were observed
(Fig. 4):
– “helicolith” horizon with Helicosphaera ampliaperta ac-
companied by other species of the genus Helicosphaera: H.
carteri, H. vedderi, H. scissura, H. euphratis and rare H. medi-
terranea (Fig. 5). Helicoliths are rarely complemented by
small placoliths of genus Reticulofenestra. Miocene speci-
mens form about 5—10 % of the taphocoenoses.
The horizon is characteristically developed in sandy clays of
the Laa Formation. On rare occasions, nearly monospecific as-
semblage with H. ampliaperta is observed. Extreme enrich-
ment (bloom) was recored in the Opatovice HJ-103 borehole
(301.7 m) where the Miocene assemblage and about 26 % of
taphocoenoses are almost exclusively formed by H. ampli-
aperta (see Fig. 3).
– horizon with Helicosphaera waltrans. Abundance of
helicoliths is slightly decreasing; they are complemented by a
low number of genera Discoaster, Calcidiscus, Umbili-
cosphaera, etc. The species Sphenolithus heteromorphus ap-
pears discontinuously and is present in very low numbers. Mi-
ocene specimens form about 10—20 % of the taphocoenoses.
The horizon was observed in clays and siliciclastic sediments
of the Grund Formation and in the basal siliciclastic sediments
of the Lower Badenian (sensu Cicha 2001). The horizon can
be subdivided into two parts :
The lower part is characterized by helicoliths with rare pres-
ence of H. waltrans (1—2 specimens/20 fields of view) and H.
ampliaperta (about 1 specimen/20—30 fields of view), and by a
discontinuous presence of H. mediterranea complemented by
rare Sphenolithus heteromorphus (1 specimen/10—20 fields of
view), Discoaster variabilis and Calcidiscus premacintyrei.
The upper part is characterized by common occurrence of H.
waltrans (5—10 specimens/10 fields of view) in association
with Helicosphaera carteri, rare H. walbersdorfensis, Reticu-
lofenestra pseudoumbilicus (< 7 µm), Calcidiscus premacinty-
rei, Discoaster variabilis, Pontosphaera multipora and Um-
bilicosphaera rotula, and by rare presence/absence of S.
heteromorphus (Figs. 6 and 7).
– horizon with Sphenolithus heteromorphus (1—5 speci-
mens/10 fields of view). The assemblage includes species of
Helicosphaera walbersdorfensis, H. carteri, Pontosphaera
multipora, Umbilicosphaera rotula, Calcidiscus premacinty-
rei, C. macintyrei, C. leptoporus, Discoaster exilis, D. variabi-
lis, a high number of small placoliths of genus Reticulofenes-
tra, large forms of Coccolithus miopelagicus (>10 µm in size),
Rhabdosphaera ssp. (sensu Young 1998) including R. sicca,
etc. Within the upper part of the interval, oval forms of species
Coronocyclus nitescens appear (localities Slavonín and Vsis-
ko), along with 5-rayed symmetrical discoasters (localities
Slavonín and Kuřim), and enigmatic specimens of genus ?Catin-
aster (or central part of discoaster?, localities Slavonín, Vsisko
and Kuřim – see Fig. 7.25,26). On rare occasions, H. medi-
terranea was observed. Miocene species form about 50—70 %
of the taphocoenoses.
The assemblage was observed in Lower Badenian clays
(“tegel”), and silty and sandy clays.
Miocene assemblages are complemented by a high number
of reworked species, mostly from the Campanian, Maastrich-
tian and Middle Eocene sediments. Reworked coccoliths and
discoasters from the Lower Cretaceous, Turonian—Coniacian
interval, Lower Paleocene (within NP2—NP3 Zones), Early
and Late Eocene, Eocene/Oligocene boundary and Oligomi-
ocene were observed in lower numbers. The quantity of re-
worked nannofossil specimens varies. Generally, taphocoenos-
es of both horizons with Helicosphaera ampliaperta and
Helicosphaera waltrans contain about 80—95 % of reworked
nannofossils whereas the proportion of reworked specimens is
distinctly decreasing in the overlying horizon with Spheno-
lithus heteromorphus, forming about 30—50 % of the tapho-
coenoses.
Discussion
The presence or absence of some stratigraphically important
forms in the Miocene sediments of the Central Paratethys is
probably controlled ecologically. According to Báldi-Beke
(1982), helicoliths are neither purely oceanic nor typical near-
shore forms. This fact influenced their expansion in the unsta-
ble paleoenvironmental conditions of the Carpathian Foredeep
and increases their significance in biostratigraphy. In the Kar-
patian and Karpatian/Badenian boundary deposits, nannofossil
assemblages are represented predominantly by helicoliths and
nearly lack specimens of other genera such as Discoaster, Um-
bilicosphaera or Sphenolithus, otherwise forming a usual
component of the assemblages.
Nannofossil species Helicosphaera waltrans was described
by Theodoridis from Gozo, Italy in 1984. This species has
Fig. 6. Miocene calcareous nannofossils of the Karpatian and Lower Badenian deposits in the Carpathian Foredeep, Moravia (Czech Repub-
lic). PPL – plane-polarized light, XPL – cross-polarized light. 1—6 – Sphenolithus heteromorphus Deflandre, Lower Badenian clays. 1—3
– Neředín No. 74; 1: PPL, 2,3: XPL at 0º and 45º; 4—6 – Hejčín, No. 28; 4: PPL, 5,6: XPL at 0º and 45º. 7—10 – Calcidiscus premacintyrei
Theodoridis, Lower Badenian clays. 7, 8 – Křelov No. K2; 7: PPL, 8: XPL; 9, 10 – Slavonín No. 50/9; 9: PPL, 10: XPL. 11, 12 – Calci-
discus cf. macintyrei (Bukry et Bramlette) Loeblich et Tappan, Lower Badenian clays. Křelov No. K2; 11: PPL, 12: XPL. 13—16 – Calcidis-
cus leptoporus (Murray et Blackman) Loeblich et Tappan, Lower Badenian clays. 13, 14 – Hejčín No. 28; 13: PPL, 14: XPL; 15, 16 –
Křelov K2; 15: PPL, 16: XPL. 17, 18 – Rhabdosphaera sicca Stradner, Lower Badenian clays. Velký Týnec No. 75; 17: PPL, 18: XPL. 19—
24 – Umbilicosphaera rotula (Kamptner) Varol, Lower Badenian clays. 19—22 – Hejčín No. 28; 19,21: PPL, 20,22: XPL; 23, 24 –
Slavonín No. 50/9; 23: PPL, 24: XPL. 25—30 – Coronocyclus nitescens (Kamptner) Bramlette et Wilcoxon, oval forms, Lower Badenian
clays. 25—28 Slavonín No. 50/8; 25,27: PPL, 26,28: XPL; 29, 30 – Vsisko No. 71; 29: PPL, 30: XPL. 31, 32 – Reticulofenestra haqii Back-
man, basal siliciclastic sediments of the Lower Badenian. Hradčany; 31: PPL, 32: XPL. 33—36 – Reticulofenestra pseudoumbilicus (Gart-
ner) Gartner, Lower Badenian clays. 33, 34 – Slavonín No. 50/7; 33: PPL, 34: XP; 35, 36 – Hejčín No. 28; 35: PPL, 36: XPL. Reworked
specimens from the Eocene and Oligocene sediments. 37, 38 – Reticulofenestra umbilicus (Levin) Martini et Ritzkowski, Lower Badenian
clays. Slavonín No. 50/9; 37: PPL, 38: XPL. 39, 40 – Pontosphaera latelliptica (Báldi-Beke) Perch-Nielsen, Lower Badenian clays. Hejčín
No. 28; 39: PPL, 40: XPL. 41, 42 – Ericsonia formosa (Kamptner) Haq, Lower Badenian clays. Slavonín No. 50/7; 41: PPL, 42: XPL. Mi-
crophotographs by L. Švábenická.
▲
204 ŠVÁBENICKÁ
CALCAREOUS NANNOFOSSILS OF THE KARPATHIAN AND BADENIAN DEPOSITS 205
Fig. 7. Miocene calcareous nannofossils of the Karpatian and Lower Badenian deposits in the Carpathian Foredeep, Moravia (Czech Repub-
lic). PPL – plane-polarized light, XPL – cross-polarized light. 1—5 – Discoaster exilis Martini et Bramlette, Lower Badenian clays. PPL;
1 – Slavonín No. 50/7; 2, 3 – Slavonín No. 50/9; 4, 5 – Neředín No. 74. 6—10 – Discoaster variabilis Martini et Bramtette, Lower Bade-
nian clay. PPL; 6 – Neředín No. 74; 7, 8 – Slavonín No. 50/8; 9, 10 – Křelov No. K2. 11 – Discoaster deflandrei Bramlette et Riedel,
Laa Formation. Opatovice HJ-103 (287.3 m); PPL. 12 – Discoaster ex gr. adamanteus Bramlette et Wilcoxon, Lower Badenian clays. He-
jčín No. 28; PPL. 13, 14 – Catinaster sp. sensu Perch-Nielsen (1985), Lower Badenian clays. Vsisko; PPL. 15 – Coccolithus miopelagicus
Bukry, Lower Badenian clays. Slavonín No. 50/8; PPL. 16—18 – Reticulofenestra minuta Roth. 16, 17 – Lower Badenian clays, Neředín
No. 74; 16: PPL, 17: XPL; 18 – Grund Formation, Šatov No. 7; XPL. 19 – Braarudosphaera bigelowii (Gran et Braarud) Deflandre, Low-
er Badenian clays. Křelov K2; PPL; specimen may be reworked from the Upper Cretaceous or Paleogene sediments. 20 – Micrantholithus
vesper Deflandre, Grund Formation. Opatovice HJ-103 (213.3 m); XPL. 21—26 – Pontosphaera multipora (Kamptner) Roth; Lower Bade-
nian clays. 21, 22 – Slavonín No. 50/8; 21: PPL, 22: XPL; 23—26 – Vsisko No. 71; 23,25: PPL, 24,26: XPL. 27—29 – Pontosphaera cf.
enormis (Locker) Perch-Nielsen, Lower Badenian clays. Vsisko No. 71; 27,28: PPL, 29: XPL; probably reworked specimen from the Oli-
gocene sediments. 30—32 – Pontosphaera discopora Schiller, Lower Badenian clays. XPL; 30 – Slavonín 50/8; 31, 32 – Neředín No. 74.
Microphotographs by L. Švábenická.
been mentioned rarely from the Miocene deposits of the Medi-
terranean and Atlantic areas only. Fornaciari et al. (1996,
1997) placed its short stratigraphic range within the middle
part of zone MNN5 (approximately middle part of Langhian),
above the Sphenolithus heteromorphus paracme/low abun-
dance interval. Young (1998: Fig. 8.2) diagrammatically ex-
pressed its short range, approximately within the middle part
of zone NN5 and correlated it with the uppermost Langhian
and lower part of the Serravalian. On the basis of quantitative
analyses, Fornaciari et al. (1996) correlated the range of H.
waltrans with the upper part of subzone MNN5a and lower
part of subzone MNN5b. According to Berggren et al. (1995),
the lower part of zone NN5 can be correlated within the “tran-
sitional” planktonic foraminiferal subzone Mt5b Praeorbulina
glomerosa/Orbulina suturalis and its middle part with zone
Mt6 Orbulina suturalis/Globorotalia peripheroronda.
In the Paratethys, H. waltrans was reported from the Lower-
Middle Miocene boundary deposits of the western part of the
Carpathian Foredeep in the area of Moravia, Czech Republic
(Švábenická & Čtyroká 1998, 1999; Čtyroká & Švábenická
1997, 2000) and Lower Austria (Švábenická 1993, 2000). H.
waltrans in rare association with Sphenolithus heteromorphus
was mentioned from the Middle Miocene sediments SE of
Kraków by Gonera & Slezak (in Ciezskowski et al. 1988;
without photodocumentation of species). In the Vienna Basin,
this species was found at the locality of Sedlecký Mlýn (E of
Mikulov, Czech Republic) by the present author, in the Slovak
part of basin by Andreyeva-Grigorovich et al. (2001) and in
the Austrian part of the basin by Coric (pers. commun.). In the
Eastern Paratethys (Crimea, Kerch Peninsula and Ukraine), H.
waltrans was recorded in a short interval of zone NN5 by An-
dreyeva-Grigorovich & Savytskaya (2000). H. waltrans has
not been mentioned from the Miocene deposits of Romania
yet, such as from the Badenian deposits of the Outer Molda-
vides (see Mărun eanu 1999). Nevertheless, the specimen pre-
sented on Fig. 5.6 is very similar in shape to H. waltrans (see
taxonomic notes in Appendix No. 1).
H. waltrans was present in the clays and coarse clastics of
the Grund Formation and in the Lower Badenian clastics of
the Carpathian Foredeep. This species was observed mostly in
the absence of Sphenolithus heteromorphus. The first occur-
rence of H. waltrans associated with rare H. ampliaperta prob-
ably coincidies with the paracme of Sphenolithus heteromor-
phus that is correlated with zone MNN4b (Fornaciari et al.
1996). The co-existence of the both species may be also ex-
plained by reworking of H. ampliaperta from the older Mi-
ocene strata. In view of the above mentioned data, H. waltrans
appears in stratigraphically older deposits of the Carpathian
Foredeep than mentioned by Fornaciari et al. (1996, 1997) and
Young (1998). The absence or rare presence of S. heteromor-
phus may also be explained ecologically. The sandy clays of
the Laa Formation, coarse clastics and clays of the Grund For-
mation and basal clastics of Lower Badenian were deposited
in temperate shallow waters, that is under conditions not
favourable for the life of sphenolith-producing Coccolitho-
phores.
Comparative studies (Čtyroká & Švábenická 1997 and
Švábenická & Čtyroká 1998, 1999) point out that the occur-
rence of H. waltrans is limited to a short stratigraphic interval
approximately corresponding to the stratigraphic range of fora-
miniferal species Globigerinoides bisphericus Todd, and in-
cluding the first appearance of Orbulina suturalis Brönnimann
in its upper part. This interval can be correlated with nanno-
plankton zones NN4 (upper part) and NN5 (lower part), that is
MNN4b and MNN5a (part) respectively (Fig. 8). Čtyroká &
Švábenická (2000) emphasized that the last occurrence of H.
waltrans precedes the last occurrence of Globigerinoides bi-
sphericus. In the Alpine-Carpathian Foredeep, Lower Austria,
H. waltrans appears before the first occurrence of G. bispheri-
cus, in association with foraminiferal microfauna Uvigerina
graciliformis Papp et Turn., Pappina parkeri breviformis
(Papp et Turn.) and rare specimens of Globorotalia (Švábe-
nická 2000).
Correlation of the first and last occurrence data of H. wal-
trans in the Carpathian Foredeep remains obscured because no
consensus exists on the correlation of the Central Paratethys
regional stages either with the Miocene standard (Mediterra-
nean) chronostratigraphic scale or with the standard nanno-
plankton NN zones (Fig. 9). The NN4/NN5 zone boundary is
attributed to the Lower/Middle Miocene (Serravalian/Lang-
hian) boundary, and to the Karpatian/Badenian boundary of re-
gional division in the Central Paratethys by Spiegler & Rögl
(1992: Table 1). Nevertheless, Rögl (1998: Table 1) and
Garecka & Olszewska (1998: Fig. 3) placed the NN4/NN5
boundary within the Langhian and the lower part of Badenian
respectively and Andreyeva-Grigorovich et al. (2001: Fig. 2)
▲
206 ŠVÁBENICKÁ
Fig. 9. Correlation of standard chronology with the Central Paratethys and Mediterranean.
Fig. 8. Comparison of nannoplankton zonation in the Mediterranean area proposed by Fornaciari et al. (1996), standard nannoplankton
zonation (Martini 1971), chronostratigraphy in the Central Paratethys and lithostratigraphy in the Carpathian Foredeep (Cicha 2001), dis-
tribution of stratigraphically significant species of planktonic foraminifers and calcareous nannofossils (Švábenická & Čtyroká 1999) and
nannoplankton horizons in the Carpathian Foredeep, Moravia (this paper).
CALCAREOUS NANNOFOSSILS OF THE KARPATHIAN AND BADENIAN DEPOSITS 207
Fig. 10. Carpathian Foredeep, southern and central Moravia. Nannopankton horizons in the Karpatian and Lower Badenian deposits shown
against NN Zones of Martini (1971) and lithology and lithostratigraphy of Cicha (2001) including the proportions of Miocene autochthonous
specimens against reworked ones in nannofossils taphocoenoses.
correlated it within the Langhian and with the Karpatian/Bade-
nian boundary. In the Mediterranean, Fornaciari et al. (1996:
Text-Fig. 17) placed the NN4/NN5 boundary within the lower
part of the Middle Miocene (lower part of the Langhian), and a
similar opinion was expressed by Berggren et al. (1995: Fig.
4) in a revised chronology of the Miocene – see Fig. 9.
H. waltrans is rarely mentioned in literature, although its
size (large helicolith about 10 µm in length), morphology
(asymmetrically elliptical outline and two triangular openings
in central area well visible under light microscope), and a short
stratigraphic range are optimum conditions for its use in bios-
tratigraphy. This “puzzle” may be caused by: 1 – The very
short stratigraphic interval where H. waltrans is available.
This is documented by Theodoridis (1984) who described the
Helicosphaera waltrans Subzone from the D.S.D.P. Site 372,
Sierra Leone Rise, Atlantic Ocean, in thickness of 6.7 m. 2 –
A taxonomic problem: in papers published before 1984, speci-
mens of H. waltrans could have been considered to be a differ-
ent, then already described species, for instance varieties of H.
mediterranea or H. sellii. This assumption is confirmed by the
study of Nagymarosy (1985: p. 78, Pl. 5, Figs. 3—6; manuscript
received in 1984) who presented specimens of H. waltrans un-
der the name Helicopontosphaera cf. sellii.
The rare occurrence of H. mediterranea in association with
H. waltrans and S. heteromorphus can by explained either by
reworking of the older Miocene strata or being a component of
the autochthonous assemblage. Báldi-Beke & Nagymarosy
(1979) and Báldi-Beke (1980) mentioned species Helico-
pontosphaera cf. sellii (syn. Helicosphaera mediterranea –
see Appendix No. 1) in association with S. heteromorphus
from the Karpatian and Badenian deposits of Central Para-
tethys, Hungary. Báldi-Beke (1982) found that the stratigraph-
208 ŠVÁBENICKÁ
ic range of H. mediterranea in the Carpathian Basin reaches
considerably higher than that in the Mediterranean or Pacific
regions, up to zone NN7. Nevertheless, H. mediterranea was
observed by Andreyeva-Grigorovich (2001) in the Vienna Ba-
sin only up to zone NN4 inclusive.
On the basis of the above mentioned observations it is possi-
ble to assume that the first occurrence of H. waltrans in the
Carpathian Foredeep probably precedes this event in the
Tethys, and that its original area of distribution was in the Cen-
tral Paratethys. This species probably migrated through the
“Trans-Tethyan-Trench-Corridor” to the Mediterranean. As
supposed by Rögl (1998) this seaway connected the Pannon-
ian, Styrian and Vienna basins and a part of the Carpathian
Foredeep. Intermittent seaways and regional closure of basins
with endemic development are supposed to occur here in the
period from the Karpatian (Late Burdigalian) to Early Bade-
nian (Langhian).
The presence of some nannofossil genera may be an impor-
tant phenomenon for the paleoclimatic and paleobathymetric
interpretations of the studied area. Aubry (1990) mentioned
Discoaster variabilis as a temperate form and D. exilis and D.
deflandrei as species that either tolerate, or exhibit preference
for colder waters. In epicontinental marine sediments, dis-
coasters are never abundant and are usually smaller in size
than in sediments deposited under oceanic conditions. In con-
trast, helicoliths are indicative for hemipelagic deposition and
they are common in shallow oceanic or epicontinental marine
deposits. Such observations can be applied also to the Car-
pathian Foredeep: a “helicolith” assemblage is observed in
sandy clays of the Laa Formation. This phenomenon indicates
a shallow epicontinental sea. Helicoliths complemented by a
low number of discoasters and coccoliths of genera Umbili-
cosphaera and Calcidiscus in clays and siliciclastic sediments
of Grund Formation and basal siliciclastic sediments of the
Lower Badenian may indicate an incipient transgression.
Higher numbers of discoasters and coccoliths recorded in the
Lower Badenian clays reflect the deepening of the deposition-
al area and open ocean conditions. Similar observations were
presented by Báldi-Beke (1980) and Nagymarosy (1985) from
the Karpatian and Badenian deposits of northern Hungary.
Conclusion
Three nannoplankton horizons were recognized in the Kar-
patian/Badenian boundary strata and in the Lower Badenian
deposits of the Carpathian Foredeep, Moravia (Fig. 10):
1. “helicolith” horizon with Helicosphaera ampliaperta,
correlated with the upper part of the Laa Formation,
2. horizon with Helicosphaera waltrans, correlated with the
Grund Formation and basal siliciclastic sediments of the Low-
er Badenian,
3. horizon with Sphenolithus heteromorphus, observed in
the Lower Badenian deposits.
The species Helicosphaera waltrans is present in a signifi-
cant horizon that is suitable for biostratigraphic use in the Car-
pathian Foredeep. The horizon is limited to a short strati-
graphic interval which approximately corresponds to the strati-
graphic range of foraminiferal species Globigerinoides bi-
sphericus and includes the first appearance of Orbulina sutu-
ralis in its upper part (Švábenická & Čtyroká 1999). This in-
terval may be correlated with the nannoplankton zones NN4
(upper part) and NN5 (lower part), that is MNN4b and the
lower part of MNN5 respectively.
The short stratigraphic range of H. waltrans seems to be dia-
chronous, first occurring in the Central Paratethys. This phe-
nomenon has to be considered carefully because no consensus
exists on the correlation of Central Paratethys regional stages
either with the Miocene standard chronostratigraphic scale or
with the nannoplankton NN zones.
The dominant occurrence of helicoliths in sandy clays of the
Laa Formation gives evidence for a shallow epicontinental
sea. The high number of helicoliths complemented by rare dis-
coasters and other coccoliths in clays and siliciclastic sedi-
ments of the Grund Formation and basal siliciclastic sediments
of the Lower Badenian may indicate a beginning of transgres-
sion.
The change in quality and quantity of Miocene nannofossil
assemblages, that is enrichment in discoasters and coccoliths
is evidence of open-sea conditions and reflects transgression
in the Lower Badenian.
Acknowledgment: This study is a contribution to the projects
“Biostratigraphy and sedimentology of the Lower and Middle
Miocene in the Alpine-Carpathian Foredeep (Lower Austria,
Moravia)” (Grant No. 205/98/0694) and “Reedition of the
Karpatian stratotype” (Grant No. 205/01/0085), supported by
the Grant Agency of the Czech Republic. The author thanks
Assoc. Prof. Dr. Ivan Cicha (Czech Geological Survey) for his
critical comments to stratigraphy in the Central Paratethys and
Dr. Eva Halásová and Prof. Dr. Aida S. Andreyeva-Grigoro-
vich (Faculty of Science, Comenius University Bratislava) for
fruitful discussions.
Appendix No. 1
Taxonomic notes
Helicosphaera mediterranea Müller
Fig. 5.13—16
Helicoponthosphaera cf. sellii Bukry et Bramlette – Báldi-Beke
(1980), p. 174, Plate IV, Figs. 17—20.
Helicosphaera mediterranea n.sp. – Müller (1981), p. 428, Pl. 1, Figs.
13,14.
Helicosphaera mediterranea Müller – Theodoridis (1984), Pl. 20,
Figs. 5—9.
Helicosphaera mediterranea Müller – Fornaciari & Rio (1996), Pl. 1,
Fig. 15.
Helicosphaera mediterranea Müller – Mărun eanu (1999), Pl. IA, Fig.
4a,b, non Pl. IB, Fig. 6.
Helicosphaera cf. waltrans Theodoridis – Andreyeva-Grigorovich &
Savytskaya (2000), Pl. I, Fig. 4.
Helicosphaera mediterranea Müller – Andreyeva-Grigorovich et al.
(2001), Fig. 4/6.
R e m a r k: In the Carpathian Foredeep, this species was record-
ed up to the lower part of zone NN5. Nevertheless, in the Grund
Formation and the overlying Lower Badenian strata, H. mediterra-
nea occurs very rarely or is absent.
CALCAREOUS NANNOFOSSILS OF THE KARPATHIAN AND BADENIAN DEPOSITS 209
Aubry (1990) drew attention to the broad geographical distribu-
tion of H. mediterranea and to the fact that its stratigraphic range
changes depending on the specific location: this species is present in
zones NN2 and NN3 in the Mediterranean, in the range of NN3—
NN5 in the Pacific and in zones NN1—NN7 in the Carpathian basins
(according to the observations of Báldi-Beke 1982).
Helicosphaera waltrans Theodoridis
Fig. 5.19—30
Helicosphaera waltrans n.sp. – Theodoridis (1984), p. 124, Pl. 13,
Fig. 2, Pl. 20, Figs. 5—9, Pl. 26, Fig. 2.
Helicopontosphaera cf. sellii Bukry et Bramlette – Nagymarosy
(1985), Pl. 5, Figs. 3—6.
Helicosphaera waltrans Theodoridis – Fornaciari et al. (1996), Pl. 2,
Figs. 11, 12.
Helicosphaera waltrans Theodoridis – Young (1998), Pl. 8.1, Fig. 18.
?Helicosphaera mediterranea Müller – Mărun eanu (1999), Pl. IB,
Fig. 6.
Helicosphaera waltrans Theodoridis – Andreyeva-Grigorovich &
Savytskaya (2000), Pl. II, Fig. 3.
R e m a r k: In the Carpathian Foredeep, this species occurs in a
stratigraphically short interval probably correlated with zones
MNN4b and a lower part of MNN5. It forms a significant horizon
that includes the Grund Formation and the basal siliciclastic sedi-
ments of the Lower Badenian. This species has not been observed in
the overlying Lower Badenian clays (“tegel”) yet.
Although Mărun eanu (1999) did not mention H. waltrans from
the Outer Moldavides, East Carpathians, the specimen depicted on
the Fig. 5.6 looks similar to H. waltrans by its elliptical outline, size
and central area where two triangular central openings are separated
by the inclined bridge.
Appendix No. 2
Nannofossil taxa mentioned in the text, in alphabetical order of
genera epithets.
Calcidiscus leptoporus (Murray et Blackman) Loeblich et Tappan
Calcidiscus premacintyrei Theodoridis
Coccolithus miopelagicus Bukry
Coronocyclus nitescens (Kamptner) Bramlette et Wilcoxon
Discoaster adamanteus Bramlette et Wilcoxon
Discoaster deflandrei Bramlette et Riedel
Discoaster exilis Martini et Bramlette
Discoaster variabilis Martini et Bramlette
Helicosphaera ampliaperta Bramlette et Wilcoxon
Helicosphaera carteri (Wallich) Kamptner
Helicosphaera mediterranea Müller
Helicosphaera scissura Müller
Helicosphaera vedderi Bukry
Helicosphaera walbersdorfensis (Müller) Theodoridis
Helicosphaera waltrans Theodoridis
Pontosphaera multipora (Kamptner) Roth
Reticulofenestra haqii Backman
Reticulofenestra minuta Roth
Reticulofenestra pseudoumbilicus (Gartner) Gartner
Rhabdosphaera sicca Stradner
Sphenolithus heteromorphus Deflandre
Umbilicosphaera rotula (Kamtner) Varol
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