MICROFOSSILS OF THE ALBIAN AND CENOMANIAN SHALES
FROM THE TRAMBERK AREA (SILESIAN UNIT,
OUTER WESTERN CARPATHIANS, CZECH REPUBLIC)
MARCELA SVOBODOVÁ
1
, LENKA HRADECKÁ
2
, PETR SKUPIEN
3
and LILIAN VÁBENICKÁ
2
1
Institute of Geology, Academy of Sciences of the Czech Republic, Rozvojová 135, 165 00 Praha 6, Czech Republic;
msvobodova@gli.cas.cz
2
Czech Geological Survey, Klárov 131/3, 118 21 Praha 1, Czech Republic; hradecka@cgu.cz; svab@cgu.cz
3
Technical University Ostrava, 17. listopadu, 708 33 Ostrava, Czech Republic; skupien@vsb.cz
(Manuscript received March 5, 2003; accepted in revised form October 2, 2003)
Abstract: Microbiostratigraphic study of sporomorphs, dinoflagellate cysts, foraminifers and calcareous nannofossils
documented the age and paleoenvironmental features of black and grey-green, organic-rich sediments in the classical
area of tramberk (Baka Formation, Silesian Unit, Outer Western Carpathians). Age-assessments suggest Late Albian
and Cenomanian age (foraminiferal Zones Rotalipora appenninica, R. reicheli and R. cushmani; nannoplankton Zones
BC27/UC0-UC4). The character of dinoflagellate cyst assemblages (e.g. presence Pterodinium) reflects open-sea envi-
ronment. The presence of calcareous foraminifers and nannofossils gives an evidence of depositional conditions above
the carbonate compensation depth (CCD). The presence of some terrestrial and non-marine aquatic palynomorphs (e.g.
Tetraporina, Lecaniella) documents the proximity of a continent and fluvio-lacustrine influences. The presence of mi-
crofossils tolerating low-oxygen bottom conditions such as foraminifers of genus Lingulogavelinella and jaws of
polychateous annelids (scolecodonts) reflect a dysaerobic bottom environment. Co-occurrence of Boreal and Tethyan
species encountered in foraminiferal and palynomorph assemblages documents the influences from the higher latitudes
on the depositional area of northern Tethys. Moreover, Lower-?Middle Cenomanian sporomorphs (angiosperms) have
similar character to others of the same age from the Blansko Graben, in the SE part of the Bohemian Cretaceous Basin,
which is situated on the SE border of the West European plate.
Key words: Cretaceous, Outer Western Carpathians, palynomorphs, foraminifers, calcareous nannofossils, biostratigra-
phy, paleoecology.
Introduction
The Cretaceous sediments of the Silesian Unit have been stud-
ied by many authors since the 19
th
century and the great atten-
tion was paid to their biostratigraphic evaluation. However, no
integrated microfossil study has been presented from the
tramberk area so far, and calcareous nannofossils from this
area have not been studied at all. This study presents the re-
sults of an integrated biostratigraphic and paleoecological
analysis of the Albian-Cenomanian deposits from the
tramberk vicinity. The tramberk Limestone and associated
Lower Cretaceous sediments in the vicinity of Oppels and
Zittels classic tramberk locality form isolated tectonic slices
grouped within three complexes Kotouè, Skalky and
Trúba. The studied microfossils come from the deposits of the
main quarry at Kotouè Hill near tramberk (Moravskoslezské
Beskydy Mts, NW Moravia, Czech Republic; Figs. 1, 2). The
associations of marine and land-derived microfossils in the
sediments of the AlbianCenomanian age from the Kotouè
Quarry near tramberk provide an opportunity to compare
marine and non-marine biostratigraphic schemes.
Geological setting
The Silesian Unit represents a middle nappe in the structure
of the Outer Western Carpathians in Moravia, which was
thrust over the Subsilesian Nappe, a part of Miocene fill of the
Carpathian Foredeep and Variscides of the Bohemian Massif
from East to West. The Silesian Unit is formed by Upper Ju-
rassic to Oligocene-Miocene deposits. Three main develop-
ments were recognized in the structure of the Silesian Unit
(Eliá 1970): the Godula development (basinal setting), Baka
development (frontal slope setting) and Kelè development
(continental setting). The Godula development (JurassicOli-
gocene) consists of deep basinal sediments (maximum thick-
ness up to 6000 m). The Baka development (Matìjka & Roth
1949, 1955; Roth et al. 1962) is characterized by shallow ma-
rine deposits.
The tramberk sequence, representing the Baka develop-
ment (Menèík et al. 1983), is part of the tectonic megaslices
(klippen) embedded within the front of the Silesian Unit. The
klippen were probably detached from the autochthonous cover
of the eastern slopes of the Bohemian Massif during
overthrusting. The reef core, reef talus and reef breccia can be
distinguished in the tramberk Limestone representing a part
of the original reef complex, which probably bordered the SE
margin of the West European plate. Many clefts, open joints
and cavities in the limestone are filled with different clayey
limestones and claystones (Figs. 2, 3). Dark grey claystones
with pyrite concretions described as the upper part of the
Plaòava Formation (Houa 1976) and as the Kotouè facies
(equivalent of the Baka Formation; Fig. 4; Pícha et al. in
print) were the object of this study.
GEOLOGICA CARPATHICA, 55, 5, BRATISLAVA, OCTOBER 2004
371388
372 SVOBODOVÁ, HRADECKÁ, SKUPIEN and VÁBENICKÁ
Although the site has been intensively studied, the hypoth-
eses concerning the origin of the limestone accumulation dif-
fer substantially. According to the first interpretation (Houa
1976; Houa in Menèík et al. 1983; Houa 1987), the bodies
of the tramberk Limestone represent a continuous strati-
graphic section, though rotated, and Olivetská hora and
Kopøivnice Limestones and clay-dominated sediments repre-
sent the Lower Cretaceous cover. According to the second in-
terpretation (Eliá & Stráník 1963; Eliá & Eliáová 1965), the
limestone bodies represent a huge oligostrome deposited dur-
ing the Early and middle Cretaceous. The deposits are as-
signed to the Tìín-Hraditì and Baka Formations (Pícha et
al. in print).
Previous studies
The origin of the lithologically variable fills of the fissures
in the tramberk Limestone is explained as a matrix of con-
glomerate composed of huge blocks and olistoliths of the
tramberk Limestone (Eliá & Stráník 1963; Eliá & Eliáová
1965). The sediments of the Kotouè Member are supposed to
be of the ValanginianTuronian age (Eliá 1970, 1983). The
sediments of the Plaòava Formation were dated to the Early
ValangianianEarly Hauterivian (Houa & Vaíèek 1996),
and Hauterivian (Hanzlíková 1962; Hanzlíková & Roth 1962;
Vavrdová 1964a,b, 1981). The age of the fills of fissures and
depressions in the limestone was indicated as Hauterivian on
the basis of macroflora by Hlutík (1979) and on the basis of
microflora by Vavrdová (1964a,b). HauterivianEarly
Barremian fauna was found in the fills of fissures by Houa
(Houa in Menèík et al. 1983; Houa 1987). The palyno-
morphs of the same age were described by Svobodová (1998).
The dinoflagellate assemblages of the Cenomanian age from
tramberk (Silesian Unit) and from the Strá Block of the Bo-
hemian Cretaceous Basin (Peruc-Korycany Formation, bore-
holes of the Uranium Industry) were compared by Svobodová
& Vavrdová (1987). Hanzlíková (1973) described the
CenomanianTuronian foraminiferal assemblage from the
Godula development. Most recently, dinocysts from the
Godula development of the Silesian Unit were studied by
Skupien (1997,1999a,b), Skupien et al. (2002) and Skupien &
Vaíèek (2003). Calcareous nannofossils of Early Barremian
age were found in the Tìín-Hraditì Formation (Krejèí et al.
1999), and those of TuronianConiacian age were found in
conglomerates near Starý Jièín (Stráník et al. 1997).
Material
All microfossil groups were studied from the same set of
samples (sporomorphs were studied by Svobodová, dinocysts
by Skupien, foraminifers by Hradecká, calcareous nanno-
fossils by vábenická). Material was obtained from the iso-
lated fissure fillings and from the depressions of dark grey to
black deposits in the tectonically deformed tramberk Lime-
stone of the Kotouè Quarry (Fig. 2). These deposits are mainly
represented by dark grey and green-grey claystones and marl-
stones rich in organic matter (Fig. 3). They are known from
isolated sites only (Fig. 3), no continuous exposures of these
deposits have been found yet. Coding of the samples consists
Fig. 1. A sketch map of the structural outline of the Silesian Unit
with indicated locality.
Fig. 2. tramberk Kotouè Quarry with some clayey fills (level
VIII) in the tramberk Limestone (state in 2002). Photo R. Kahánek.
Fig. 3. Detail of fissure in the Kotouè Quarry, sample 2/VIII. Photo
M. Svobodová.
MICROFOSSILS OF THE SHALES FROM TRAMBERK (OUTER WESTERN CARPATHIANS) 373
?
PA
L.
Danian
Maastrichtian
Campanian
Santonian
Coniacian
Palkovice
Formation
Turonian
?
U
pper
Cenomanian
Baka
Formation
Chlebovice
Member
Albian
Aptian
Barremian
Hauterivian
K
oto
uè F
ac
ie
s
TìínHraditì
Formation
Valanginian
Kopøivnice Limestone
C
R
E
T
A
C
E
O
U
S
Lo
wer
Berriasian
JUR
.
Tithonian
tramberk Limestone
IIIIIIIIIIIIIII
of three parts: the first denotes the sampling site (tramberk
), the second denotes the sample number in Arabic numerals
(e.g. 2), and the third part denotes the quarry level in Roman
numerals (e.g. VIII). The location of the studied samples is
given by the general position system GPS (Fig. 5).
Methods
Palynological preparations were obtained using a standard
procedure involving mineral acid treatment (10% HCl, 40%
HF, acetolysis, 30% HNO
3
). One part of the residue was
sieved using 10 µm mesh with ultrasonic vibration in order to
dissolve and decompose amorphous organic matter. Qualita-
tive analyses of palynomorph associations were based on
counts of 200 sporomorphs and 200 dinoflagellate cysts per
sample. The weight of collected samples for the study of fora-
minifers was about 0.751 kg. The samples were washed in
the Laboratory of the Czech Geological Survey using standard
washing methods and sieved at 0.063 mm sieve. Foraminifers
were separated under a binocular microscope, and photo-
graphs of species were taken using a scanning electron micro-
scope. Planktonic zonation of Robaszynski & Caron (1995)
was used for the correlation of the studied assemblages. Sus-
pension slides for calcareous nannofossil study were prepared
using a decantation method, with a separated fraction of 3
30 µm. Slides were inspected with a Nikon light microscope at
1000× magnification. Quantitative data are based on ca. 300
500 specimens. Biostratigraphic data were correlated with the
standard nannoplankton CC zones of Sissingh (1977), and
with the Lower Cretaceous Boreal nannoplankton BC zones
of Bown et al. (1998) and Upper Cretaceous nannofossil zones
of Burnett (1998).
Results
Generally, light green-grey claystones and marlstones
mostly contained foraminifers and calcareous nannofossils. In
contrast, black and grey claystones contained rich dinocysts
and sporomorphs, and usually provided poor foraminifers and
calcareous nannofossil assemblages.
Sporomorphs
Spores and pollen grains were found in samples: 2/VIII,
15/V and 49C/VIII (Figs. 6, 7, 8, 9). Dark grey claystones
filling cavities in the limestone body of the Kotouè Quarry at
tramberk yielded mostly poorly preserved sporomorph as-
semblage characterized by the occurrence of angiosperm pol-
len grains. Angiosperm pollen grains are known to appear for
the first time in the Barremian, but no angiosperm pollen
grains have been found in either the Barremian or the Albian
deposits at tramberk (dated by calcareous nannofossils and
foraminifers). Samples 2/VIII, 15/V and 49C/VIII contain
abundant trilete spores (1835 %), gymnospermous pollen (6
12 %) and rare angiospermous pollen (25 %). The quality of
sporomorph preservation in the investigated samples is vari-
able. Poor preservation was observed in samples 2/VIII and
15/V, while sample 49C/VIII provided excellent material
probably as a result of caused by sampling of non-oxidized
sediments due to rapidly advancing exploitation in the quarry.
Samples 2/VIII and 15/V yielded mainly reticulate
tricolpate pollen such as Tricolpites variabilis, T. sagax,
psilate tricolpate and tricolporate pollen (Psilatricolpites
parvulus, Psilatricolporites sp.). Monocotyledonous pollen
Liliacidites dividuus, L. variegatus, Clavatipollenites spp. pre-
Fig. 4. Lithostratigraphy of the Silesian Unit, Baka development.
From Pícha et al. (in print), modified. Jur. Jurassic, Pal. Pa-
leogene,
▲▲▲▲
tectonic detachment.
Fig. 5. Localization and lithology of the AlbianCenomanian sam-
ples. (Positions of samples were located using the GPS General
Position System. The error of the measurement was 57 meters.)
SampleNo./
level in
quarry
Latitude N Longitude E Lithological description
0/VIII
49°34´893´´ 018°06´745´´ greenish marlstone
1/VIII
49°34´902´´ 018°06´747´´ greenish marlstone
2/VIII
49°34´901´´ 018°06´745´´ grey claystone
11/VI
49°34´989´´ 018°06´871´´ grey claystone
15/V
49°34´985´´ 018°06´858´´ sandy siltstone
29/IV
49°34´998´´ 018°06´779´´ green-grey sandy claystone
30/IV
49°35´007´´ 018°06´779´´ green-grey clayey siltstone
49B/VIII 49°34´952´´ 018°07´035´´ black claystone
49C/VIII 49°34´792´´ 018°07´051´´ dark grey claystone
374 SVOBODOVÁ, HRADECKÁ, SKUPIEN and VÁBENICKÁ
vail in the angiosperm assemblage in sample
49C/VIII. All three tramberk samples consis-
tently yielded abundant spore and gymnosperm
pollen assemblages. Non-saccate forms such as
Cycadopites spp., the monoporate striate type
Corollina torosa, Eucommiidites minor, Taxo-
diaceaepollenites hiatus, and T. vacuipites are
more common than bisaccate pollen grains.
Callialasporites dampieri occurs rarely in
samples 15/V and 49C/VIII. These pollen
grains have not been found in coeval deposits of
the Bohemian Cretaceous Basin (Svobodová et
al. 1998; Svobodová & Brenner 1999). Some
pteridophyte spores found in the Cenomanian
deposits, that is, Collarisporis fuscus, Cornicu-
latisporites auritus were described by Juhász
(1983) from the Transdanubian mid-Cretaceous
formations (Tethyan Realm, Hungary) while
other sporomorphs are distributed worldwide.
Nevertherless, this phenomenon supports the
theory of mixing of Tethyan and Boreal ele-
ments in the depositional area of the Silesian
Unit.
Dinocysts
Dinocyst preservation in the studied samples
from the Kotouè Quarry at tramberk is vari-
able. The most conspicuous feature in the rela-
tive abundance diagrams (Fig. 7) is the preva-
lence of marine palynomorphs (mostly di-
noflagellates and foraminiferal linings). Di-
noflagellate cysts and acritarchs form 3847 %
and other marine faunal remains, foraminiferal
linings represent 625 %. They were found in
four samples: 2/VIII, 15/V, 49B/VIII and
49C/VIII (Figs. 10, 11). Hystrichodinium pul-
chrum, Kiokansium unituberculatum, Lito-
sphaeridium siphoniphorum, Oligosphaeridium
complex, Spiniferites ramosus and Surculo-
sphaeridium sp. prevail in the dinocyst assem-
blages of samples 2/VIII, 49B/VIII and
49C/VIII. The dinoflagellate assemblage of
sample 15/V differs markedly from previous
one in the pronounced prevalence of represen-
tatives of genus Ovoidinum. Representatives of
the genus Achomosphaera are common in all
samples. Species Pervosphaeridium pseudhyst-
richodinium, which is typical for the Late
AlbianCenomanian deposits of the Silesian
Unit, occurs only in sample 49C/VIII. This as-
semblage is comparable to that described from
the uppermost part of the Lhoty Formation
(Late Albian age) and the lower part of the var-
iegated Godula Member (Early Cenomanian
Skupien 1999b; Skupien et al. 2002).
Foraminifers
The stratigraphically youngest assemblages
of foraminifers were found in samples 0/VIII,
Fig. 6. Distribution of sporomorph taxa and some aquatic palynomorphs in the Cen-
omanian deposits of tramberk Kotouè Quarry (Baka development), Silesian
Unit. Sporomorph abundance: L low, M moderate , * rare (13), ** oc-
curs (410), *** common (1120), **** abundant (2140 specimens). Sporo-
morph preservation: VP very poor, M moderate.
SPORES, POLLEN, AQUATIC PALYNOMORPHS
Early?Middle
CENOMANIAN
Sample No.
2/VIII 15/V 49C/VIII
sporomorph abundance in slide
L
M
M
sporomorph preservation
VP
M
M
Leiofusa jurassica Cookson et Eisenack
*
*
Lecaniella sp.
*
Pterospermella australiensis (Deflandre et Cookson) Eisenack
*
Tetraporina sp.
*
Veryhachium rhomboidium Downie
*
scolecodonts
*
*
foraminiferal linings
**
****
Appendicisporites sp.
*
*
*
Biretisporites sp.
*
Camarozonosporites ambigens
*
Camarozonosporites insignis Norris
*
*
*
Cibotiumspora cf. juncta (Kara Murza) Zhang
*
Cicatricosisporites cf. proxiradiatus Kemp
*
Cicatricosisporites sp.
*
*
*
Clavifera triplex (Bolchovitina) Bolchovitina
*
*
Collarisporites fuscus Deák
*
Corniculatisporites cf. auritus (Singh) Juhász
*
Coronatispora perforata Dettmann
*
Cyathidites minor Couper
*
*
Dictyophyllidites sp.
*
Echinatisporites varispinosus (Pocock) Srivastava
*
*
Foveogleicheniidites confossus (Hedlund)
*
*
*
Foveosporites pseudoalveolatus (Couper) McKellar
*
Gleicheniidites apilobatus Brenner
*
Gleicheniidites cf. bolchovitinae Döring
*
Gleicheniidites carinatus (Bolchovitina) Bolchovitina
*
Gleicheniidites senonicus Ross emend. Skarby
***
**
**
Gleicheniidites spp.
**
*
*
Klukisporites sp.
*
Laevigatosporites ovatus Wilson et Webster
*
*
Leptolepidites psarosus Norris
*
Reticulosporites cretacius Pacltová et Krutzsch
*
Retitriletes austroclavatidites (Cookson) Döring et al. in W. Kr.
*
*
*
Retitriletes circolumenus (Cookson et Dettmann) Backhouse
*
Stereisporites antiquasporites (Wilson et Webster) Kremp
*
Retitriletes semimuris (Danzé-Corsin et Laveine) McKellar
*
Stereisporites psilatus (Ross) Pflug
*
Vadaszisporites urkuticus Juhász
*
Alisporites bilateralis Rouse
*
*
Alisporites cf. grandis (Cookson) Dettmann
*
*
Callialasporites dampieri (Balme) Sukh Dev
*
*
Corollina torosa (Reissinger) Klaus emend. Cornet et Traverse
**
*
Cycadopites cf. follicularis Wilson et Webster
*
Cycadopites fragilis Singh
*
*
Cycadopites sp. A
*
Eucommiidites minor Groot et Penny
*
*
Parvisaccites radiatus Couper
*
*
*
Parvisaccites rugulatus Brenner
*
Phyllocladidites sp.
*
*
Podocarpidites sp.
*
**
**
Pristinuspollenites cf. elongatus (Kemp) Singh
*
Taxodiaceaepollenites hiatus (Potonié) Kremp
**
**
Taxodiaceaepollenites vacuipites (Woodhouse)
*
Vitreisporites pallidus (Reissinger) Nilsson
*
*
**
Asteropollis sp.
*
Brenneripollis peroreticulatus (Brenner) Juhász
*
Clavatipollenites sp.
*
***
Liliacidites dividuus (Pierce) Brenner
*
Liliacidites variegatus Couper
*
Psilatricolpites parvulus Norris
*
*
Psilatricolporites sp.
*
*
Retitricolporites sp.
*
Tricolpites sagax Norris
*
Tricolpites variabilis Burger
*
*
Tricolporoidites sp.
*
MICROFOSSILS OF THE SHALES FROM TRAMBERK (OUTER WESTERN CARPATHIANS) 375
1/VIII, 2/VIII, 11/VI, 15/V, 29/IV, 30/IV, 49B,C/VIII.
These foraminiferal assemblages are composed of tests of ag-
glutinated, calcareous benthic and planktonic species (Fig. 12,
13). Benthos, especially calcareous benthos, prevails in all the
studied samples. The species Trocholina remesiana
(Chapman) and Turrispirillina sp. are frequent much like the
representants of genera Lingulogavelinella and Lenticulina.
The agglutinated species Marssonella oxycona (Reuss),
Arenobulimina macfadyeni Cushman, A. preslii (Reuss) and
Ammodiscus gaultinus Berthelin are common. Plankton is rep-
resented mostly by species of two genera Hedbergella, and
the stratigraphically important Rotalipora (Fig. 14, 15). Only
a few specimens of Globigerinelloides ultramicra (Subbotina)
were found in sample 2/VIII. The character of the foramin-
Fig. 7. Proportions of palynomorph groups of the Early Cenomanian
age in the dark pelitic fillings in the limestone body of the tramberk
Member (Baka development).
Fig. 8. Sporomorphs and some aquatic taxa from tramberk Kotouè Quarry. Locality name is followed by sample No. 1 Camarozono-
sporites insignis Norris; Kotouè Quarry, 15/V. 2 Stereisporites psilatus (Ross) Pflug, 1953; Kotouè Quarry, 2/VIII. 3 Gleicheniidites
bolchovitinae Döring, 1965; Kotouè Quarry, 15/V. 4 Retitriletes circolumenus (Cookson et Dettmann) Backhouse, 1978; Kotouè Quarry,
15/V. 5 Callialasporites dampieri (Balme) Sukh Dev, 1961; Kotouè Quarry, 15/V. 6 Corniculatisporites cf. auritus (Singh) Juhász, 1977;
Kotouè Quarry, 15/V. 7 Pristinuspollenites cf. elongatus (Kemp) Singh, 1983; Kotouè Quarry, 15/V. 8 Alisporites cf. grandis (Cook-
son) Dettmann, 1963; Kotouè Quarry, 15/V. 9 Cycadopites sp. A; Kotouè Quarry, 15/V. 10 Parvisaccites rugulatus Brenner, 1963;
Kotouè Quarry, 15/V.
376 SVOBODOVÁ, HRADECKÁ, SKUPIEN and VÁBENICKÁ
iferal assemblages is similar in all the studied samples (Fig.
10). Calcareous benthos prevails (4270 %), agglutinated
benthos constitutes 2040 % of the assemblage and plankton
constitutes only 1025 %. Eighteen genera from nine families
were recognized in the calcareous benthos, of which
Vaginulinidae and Gavelinellidae (sensu Loeblich & Tappan
1988) are the most common. Genera Lenticulina, Lingulo-
gavelinella, Gavelinella and Trocholina prevail in the calcare-
ous benthos foraminiferal assemblage. The agglutinated spe-
cies belong to 13 genera and 10 families, the most common of
which are Ataxophragmidae, Ammodiscidae, and Spiro-
plectamminidae. The foraminiferal species Rotalipora is a
typical single-keeled representative of the Tethyan Realm but
Boreal elements are also present (Gaudryina, Dorothia,
Gyroidinoides etc.).
Fig. 9. 1 Tetraporina sp.; Kotouè Quarry, 15/V. 2 Lecaniella sp.; Kotouè Quarry, 15/V. 3 Leiofusa jurassica Wall et al.; Kotouè
Quarry, 15/V. 4 Laevigatosporites ovatus Wilson et Webster, 1946; Kotouè Quarry, 15/V. 5 Corollina torosa (Reissinger) Klaus
emend. Cornet et Traverse; Kotouè Quarry, 49C/VIII. 6 Cibotiumspora cf. juncta (Kara-Murza) Zhang, 1978; Kotouè Quarry, 15/V. 7
Coronatispora perforata Dettmann; Kotouè Quarry, 49C/VIII. 8 Gleicheniidites senonicus Ross emend. Skarby, 1964; Kotouè Quarry,
2/VIII. 9 Taxodiaceaepollenites hiatus (Potonié) Kremp; Kotouè Quarry, 15/V. 10, 11 Tricolpites variabilis Burger, 1970; Kotouè
Quarry, 15/V. 12 Psilatricolpites parvulus Norris, 1967; Kotouè Quarry, 2/VIII.
Calcareous nannofossils
The deposits provided low- to medium-abundance, poorly
preserved calcareous nannofossil assemblages. Specimens usu-
ally show strong dissolution and mechanical damage. The cen-
tral areas of placoliths are mostly destroyed, which makes the
identification of some species difficult (Fig. 16.10,11,21). The
nannoplankton assemblages are characterized by abundant
Watznaueria barnesae, by relatively high numbers of
Eiffellithus turriseiffelii, Eprolithus floralis and Predisco-
sphaera ponticula (Fig. 17), and by the presence of large
broadly elliptical specimens of Manivitella pemmatoidea (Fig.
16.25). Specimens of Corrolithion kennedyi, Lithraphidites
acutus and Gartnerago theta occur rarely. High species diver-
sity is displayed by the genera Zeugrhabdotus and Watznaueria.
MICROFOSSILS OF THE SHALES FROM TRAMBERK (OUTER WESTERN CARPATHIANS) 377
DINOFLAGELLATE CYSTS
Latest ALBIAN
Early
CENOMANIAN
Sample No.
2/VIII
15/V
49B/VIII
49C/VIII
Achomosphaera neptunii (Eisenack) Davey et Williams
x
x
x
x
Achomosphaera ramulifera (Deflandre) Evitt
x
x
x
Achomosphaera triangulata (Gerlach) Davey et Williams
x
x
x
Callaiosphaeridium asymmetricum (Deflandre et Courteville) Davey et Williams
x
Circulodinium brevispinosum (Pocock) Jansonius
xx
Circulodinium distinctum (Deflandre et Cookson) Jansonius
xx
xx
x
x
Cleistosphaeridium? multispinosum (C. Singh) Brideaux
x
Cometodinium habibii Monteil
x
Cometodinium? whitei (Deflandre et Courteville) Stover et Evitt
x
x
x
Coronifera oceanica Cookson et Eisenack
x
Cribroperidinium orthoceras (Eisenack) Davey
x
x
Cymososphaeridium validum Davey
x
Dapsilidinium multispinosum (Davey) Bujak et al.
x
Endoscrinium cf. campanula (Gocht) Vozzhennikova
x
x
Exochosphaeridium sp.
x
xx
x
x
Florentinia cooksoniae (C. Singh) Duxbury
x
Florentinia laciniata Davey et Verdier
x
Florentinia stellata (Maier) Below
x
Epelidosphaeridia spinosa Cookson et Hughes
x
Fromea amphora Cookson et Eisenack
x
x
Gonyaulacysta cf. cassidata (Eisenack et Cookson) Sarjeant
x
Gonyaulacysta sp.
x
Heterosphaeridium sp.
xx
Hystrichodinium pulchrum Deflandre
xx
x
xx
Hystrichosphaeridium sp.
x
Hystrichostrongylon membraniphorum Agelopoulos
Kiokansium unituberculatum (Tasch) Stover et Evitt
xx
xx
Kiokansium sp.
xx
x
Kleithriasphaeridium eoinodes (Eisenack) Davey
x
x
x
Kleithriasphaeridium fasciatum Davey et Williams
x
Leberidocysta chlamydata Cookson et Eisenack
Litosphaeridium arundum (Eisenack et Cookson) Davey
x
Litosphaeridium siphoniphorum (Cookson et Eisenack) Davey et Williams
x
xx
xx
Odontochitina operculata (O. Wetzel) Deflandre et Cookson
xx
x
x
x
Oligosphaeridium? asterigerum (Gocht) Davey et Williams
x
x
xx
Oligosphaeridium complex (White) Davey et Williams
xx
xx
xx
xx
Ovoidinium scabrosum (Cookson et Hughes) Davey
xxx
Ovoidinium verrucosum (Cookson et Hughes) Davey
xx
Palaeohystrichophora infusorioides Deflandre
x
x
xx
Pervosphaeridium pseudhystrichodinium (Deflandre) Yun
xx
Pervosphaeridium truncatum (Davey) Below
x
Prolixosphaeridium sp.
x
Protoellipsodinium spinocristatum Davey et Verdier
x
Pterodinium cingulatum (O. Wetzel) Below
xx
x
Spiniferites ramosus (Ehrenberg) Mantell
xxx
x
xx
Spiniferites sp.
xx
x
Surculosphaeridium? longifurcatum (Firtion) Davey et al.
x
x
Surculosphaeridium sp.
xx
x
Systematophora diversispinosa (Davey et al.) Islam
xx
Systematophora sp.
x
x
Tanyosphaeridium sp.
x
x
Xiphophoridium alatum (Cookson et Eisenack) Sarjeant
x
Wallodinium krutzschii (Alberti) Habib
x
x
The quantity and diversity vary among the samples (Fig.
17). The most abundant assemblage with well preserved
coccoliths was found in greenish marlstone (1/VIII) and dark
grey claystone (49C/VIII) whereas the claystones of samples
49B/VIII, 2/VIII, 30/IV and 29/IV provided rare and
poorly preserved nannofossil specimens. The sandy siltstone
(15/V) contains no calcareous nannofossils.
Biostratigraphy
Age interpretation of the studied samples was determined
on the basis of the presence of index microfossils. The se-
lected specimens are plotted at Fig. 18.
Sample 11/VI
The foraminiferal assemblage is characterized by the preva-
lence of genera Lingulogavelinella and Lenticulina, plank-
tonic foraminifers are represented by genus Hedbergella sp.
exclusively. This feature gives the evidence of the Late
AlbianCenomanian interval. The presence of the nannofossil
species Eiffellithus turriseiffelii and the absence of the
Cenomanian taxa indicate the latest Albian. No palynomorphs
have been found.
Sample 49B/VIII
Both foraminiferal and nannofossil assemblages have a
similar character to the previous sample 11/VI. The di-
noflagellate cysts with Palaeohystrichophora infusorioides
Fig. 10. Distribution of dinoflagellate cysts in the Albian-Cenomanian deposits of tramberk, Silesian Unit (x less than 4 %, xx 45%,
xxx 1530%, xxxx more than 30 %).
378 SVOBODOVÁ, HRADECKÁ, SKUPIEN and VÁBENICKÁ
Fig. 11. Dinoflagellate cysts from tramberk. The species name is followed by the size of the specimen, sample location and England Finder
coordinates. 1 Circulodinium distinctum (Deflandre et Cookson, 1955) Jansonius, 1986; body width 80 µm, 2/VIII-b, K27/28. 2 Sur-
culosphaeridium sp.; body diameter 60 µm, 2/VIII-g, W36/1. 3 Ovoidinium verrucosum (Cookson et Hughes, 1964), Davey, 1970; length
60 µm, 15/V-a, N/O33. 4 Fromea amphora Cookson et Eisenack, 1958; length 45 µm, 15/V-c, T36/1. 5 Achomosphaera ramulifera
(Deflandre, 1937) Evitt, 1963; length 62 µm, 15/V-c, P25. 6 Pervosphaeridium pseudhystrichodinium (Deflandre, 1937) Yun, 1981;
length 87 µm, 2/VIII-b, K28. 7 Kleithriasphaeridium eoinodes (Eisenack, 1958) Davey, 1974; length 77 µm, 2/VIII-b, M18/19. 8, 11
Odontochitina operculata (O. Wetzel, 1933) Deflandre et Cookson, 1955; 8. free operculum, length 114 µm, 2/VIII- h, B31/1; 11. length
105 µm, 2/VIII-f, S/T28. 9 Litosphaeridium siphoniphorum (Cookson et Eisenack, 1958) Davey et Williams, 1966; diameter 43 µm,
15/V-a, T/U41. 10 Xenascus sp.; length 63 µm, 2/VIII-f, J45/1. 12 Florentinia laciniata Davey et Verdier, 1973; diameter 65 µm,
2/VIII-f, T28.
MICROFOSSILS OF THE SHALES FROM TRAMBERK (OUTER WESTERN CARPATHIANS) 379
and Litosphaeridium siphoniphorum indicate the latest
AlbianEarly Cenomanian. No sporomorphs have been found.
Sample 15/V
The foraminiferal assemblage is similar to that from
samples 11/VI and 49B/VIII indicating the Late Albian
Cenomanian interval. The dinoflagellate cysts with
Ovoidinium scabrosum, Ovoidinium verrucosum and
Protoellipsodinium spinocristatum indicate an age not
younger than Upper Albian. Both nannofossils with
Corrolithion kennedyi (UC1-UC2 Zone) and the high number
Late Albian - Cenomanian
Middle Cenomanian
M-L.C
Rotalipora appenninica - R.cushmani Zone
Rotalipora reicheli Zone
R.cushmani
Zone
FORAMINIFERA
Sample No.
11/VI 49B/VIII 0/VIII
15/V 49C/VIII 30/IV
29/IV
1/VIII
2/VIII
Ammobaculites sp.
xx
Ammobaculoides lepidus Hercogová
x
Ammodiscus gaultinus Berthelin
x
x
xx
Arenobulimina macfadyeni Cushman
x
x
x
x
x
Arenobulimina preslii (Reuss)
x
x
xx
Arenobulimina sp.
x
Ataxophragmium sp.
x
x
Dorothia filiformis (Berthelin)
x
Dorothia turris (d´Orbigny)
x
Gaudryina trochus (d´Orbigny)
x
x
Gaudryina dispanza Chapman
x
Glomospira irregularis (Grzybowski)
x
Haplophragmoides latidorsatus (Borne.)
x
Marssonella oxycona (Reuss)
x
xx
xx
x
Spiroplectammina scotti Cushm.-Alex.
x
Textularia foeda Reuss
x
Tritaxia plummerae Cushman
x
a
gg
lu
tin
at
ed
b
en
th
os
Trochammina sp.
x
Astacolus sp.
x
x
x
Dentalina sp.
x
x
x
x
Gavelinella baltica Brotzen
x
Gavelinella cf. cenomanica (Brotzen)
x
x
Gavelinella sp.
x
Globorotalites sp.
x
x
Gyroidinoides infracretacea Morozova
x
x
x
Hemirobulina linearis (Reuss)
x
Laevidentalina sororia (Reuss)
x
Lenticulina gaultina (Berthelin)
x
Lenticulina sp.
x
x
x
x
x
Lingulogavelinella globosa (Brotzen)
x
xx
x
L.albiensis arachnoidea Gawor-Biedowa
x
x
Lingulogavelinella jarzevae Vasilenko
xx
xx
x
x
Lingulogavelinella pazdroae Gawor-B.
xx
x
xx
x
Marginulina elongata d´Orbigny
x
Neobulimina minima Tappan
x
x
Pleurostomella reussi Berthelin
x
x
Praebulimina avexa (Loeblich et Tappan)
x
x
Psilocitharella recta (Reuss)
x
Ramulina laevis Jones
x
x
x
Saracenaria triangularis (dOrbigny)
x
Trocholina remesiana (Chapman)
xxx
Trocholina solecensis Bielecka et Poar.
x
c
al
ca
re
ou
s b
en
th
os
Turrispirillina sp.
x
x
x
x
x
x
Globigerinelloides ultramicra (Subbotina)
x
xx
Hedbergella delrioensis (Carsey)
x
x
x
x
x
xx
Hedbergella portsdownensis (Will.-Mit.)
x
Hedbergella planispira (Tappan)
x
x
x
x
Hedbergella simplex (Morrow)
x
x
x
Rotalipora appenninica (Renz)
x
Rotalipora brotzeni (Sigal)
x
x
x
Rotalipora cushmani (Morrow)
x
Rotalipora greenhornensis (Morrow)
x
x
xx
Rotalipora reicheli Mornod
x
x
xx
p
la
nk
to
n
Ticinella sp.
x
x
Fig. 13. Proportions of groups of foraminifers (in %) from the
studied samples from the Kotouè Quarry.
Fig. 12. Distribution of foraminifers in the Albian-Cenomanian deposits of tramberk, Silesian Unit.
380 SVOBODOVÁ, HRADECKÁ, SKUPIEN and VÁBENICKÁ
Fig. 14. Foraminifers from tramberk Kotouè Quarry. Species name is followed by sample No. 1 Turrispirillina sp., 0/VIII. 2 As-
tacolus sp., 1/VIII. 3 Lingulogavelinella pazdroae Gawor-Biedowa, 0/VIII. 4 Lingulogavelinella globosa (Brotzen), 0/VIII. 5
Lingulogavelinella jarzevae Vasilenko, 11/VI. 6 Ammobaculoides lepidus Hercogová, 1/VIII. 7 Ammodiscus gaultinus Berthelin,
1/VIII. 8 Ammobaculites sp., 1/VIII. 9 Pleurostomella reussi Berthelin, 1/VIII. 10 Arenobulimina preslii (Reuss), 1/VIII. 11
Lingulogavelinella albiensis arachnoidea Gawor-Biedowa, 0/VIII. 12 Dorothia turris (dOrbigny), 0/VIII. 13 Gavelinella cf.
cenomanica (Brotzen), 11/VI. 14 Dentalina sp., 1/VIII. 15 Neobulimina minima Tappan, 0/VIII. 16 Globorotalites sp., 1/VIII.
Scale bars = 100 µm.
MICROFOSSILS OF THE SHALES FROM TRAMBERK (OUTER WESTERN CARPATHIANS) 381
Fig. 15. 1 Ticinella sp., 11/VI. 2 Rotalipora? sp., 1/VIII. 3 Globigerinelloides ultramicra (Subbotina), 2/VIII. 4 Hedbergella
planispira (Tappan), 2/VIII. 5 Hedbergella simplex (Morrow), 1/VIII. 6 Hedbergella portsdownensis (Williams-Mitchell), 0/VIII.
7 Hedbergella cf. simplex (Morrow), 1/VIII. 8 Hedbergella delrioensis (Carsey), 1/VIII. 9 Rotalipora reicheli Mornod, 1/VIII.
10 Rotalipora brotzeni (Sigal), ventral view, 1/VIII. 11 Rotalipora reicheli Mornod, 1/VIII. 12 Rotalipora appenninica (Renz),
ventral view, 1/VIII. 13 Rotalipora cushmani (Morrow), 2/VIII. 14 Rotalipora greenhornensis (Morrow), 1/VIII. 15 Rotalipora
appenninica (Renz), dorsal view, 0/VIII. Scale bars = 50 µm.
382 SVOBODOVÁ, HRADECKÁ, SKUPIEN and VÁBENICKÁ
Fig. 16. Stratigraphically significant calcareous nannofossils from the tramberk Quarry, Silesian Unit, Outer Western Carpathians. PPL
plane-polarized light; XPL cross-polarized light. 1, 2 Tranolithus orionatus (Reinhardt) Reinhardt; 1: PPL, 2: XPL. 3, 4 Helenea
chiastia Worsley; 3: PPL, 4: XPL. 5, 6 Chiastozygus litterarius (Górka) Manivit; 5: PPL, 6: XPL. 79 Eprolithus floralis (Stradner)
Stover; 7: PPL, 8 and 9: XPL. 10 Eiffellithus turriseiffelii Reinhardt; XPL. 11, 12 Axopodorhabdus albianus (Black) Wind et Wise;
11: PPL, 12: XPL. 13, 14 Gartnerago theta (Black) Jakubowski; 13: PPL, 14: XPL. 1517 Corollithion kennedyi Crux; 15: PPL, 16
and 17: XPL. 18 Watznaueria biporta Bukry; XPL. 19, 20 Prediscosphaera cretacea (Arkhangelsky) Gartner; 19: PPL, 20: XPL. 21,
22 Prediscosphaera ponticula (Bukry) Perch-Nielsen; 21: PPL, 22: XPL. 23, 24 Zeugrhabdotus embergerii (Noël) Perch-Nielsen; 23:
PPL, 24: XPL. 25, 26 Manivitella pemmatoidea (Deflandre) Thierstein; 25: PPL, 26: XPL.
of angiosperm pollen grains with Psilatricolporites sp.,
Brenneripollis peroreticulatus, Liliacidites variegatus and
Liliacidites dividuus indicate the Early?Middle Cenoman-
ian age.
Sample 30/IV
The presence of the foraminiferal species Rotalipora reicheli
indicates the Middle Cenomanian age (Rotalipora reicheli
Zone). The nannoplankton assemblage is similar to that one
found in sample 49C/VIII and gives evidence of an Early-
?Middle Cenomanian age. No palynomorphs were found.
Samples 29/IV and 1/VIII
Both the foraminifers and nannofossils correspond to the
Middle Cenomanian. The foraminiferal association has the
same character as the assemblage from sample 30/IV.
MICROFOSSILS OF THE SHALES FROM TRAMBERK (OUTER WESTERN CARPATHIANS) 383
Fig. 17. Distribution of nannofossil taxa in the Upper Albian and Cenomanian deposits of tramberk Quarry, Silesian Unit, Outer Western Car-
pathians. Abundance of nannofossil taxa: A abundant (>10%), C common (510%), F few (15 %), R rare (<1%), ? question-
able species, r reworked species from older strata. Abundance of nannofossil specimens in sample: H high (>30 specimens per field of
view of microscope), M moderate (1030 specimens per field of view), L low (<10 specimens per field of view). Preservation of nanno-
fossils in sample: M moderate (overgrowth and etching is apparent but the majority of specimens are easily identifiable), P poor (over-
growth and etching is intensive making identification of some specimens difficult), VP very poor (some specimens cannot be identified).
ALBIAN
C E N O M A N I A N
CALCAREOUS NANNOFOSSILS
Late
Early
Early-Middle
?Middle-Late
Calcareous nannofossil zones
BC27/UC0
UC1-?UC3a
?UC3-UC4
BC (Bown 1998); UC (Burnett 1998)
a-b
b
c
Sissingh (1977)
CC9a-b
CC9c
CC10a
Sample No.
11/VI 49B/VIII 0/VIII
2/VIII 49C/VIII 30/IV
29/IV
1/VIII
nannofossil abundance in sample
L
L
M
L
H
L
L
H
nannofossil preservation
P
VP
P
VP
M
VP
VP
M
Axopodorhabdus albianus (Black) Wind et Wise
R
F
F
R
R
F
Biscutum ellipticum (Górka) Grün
F
R
R
R
F
Broinsonia enormis (Shumenko) Manivit
R
R
R
R
R
Broinsonia signata (Noël) Noël
R
R
F
F
R
R
Chiastozygus litterarius (Górka) Manivit
R
R
Corollithion kennedyi Crux
F
R
Cretarhabdus conicus Bramlette et Manivit
R
R
R
Cretarhabdus striatus (Stradner) Black
R
f
R
?Cribrosphaerella sp.
R
Cyclagelosphaera cf. margerelii Noël
R
R
Cyclagelosphaera reinhardtii (Perch-Nielsen) Romein
R
R
R
Discorhabdus ignotus (Górka) Perch-Nielsen
R
Eiffellithus monechiae Crux
R
Eiffellithus striatus (Black) Applegate et Bergen
R
R
Eiffellithus turriseiffelii (Deflandre) Reinhardt
F
F
R
C
F
R
C
Eprolithus floralis (Stradner) Stover
R
R
C
F
F
C
F
Gartnerago theta (Black) Jakubowski
R
R
R
Grantarhabdus coronadventis (Reinhardt) Grün
R
Haqius circumradiatus (Stover) Roth
R
R
R
Helenea chiastia Worsley
R
F
F
F
R
R
R
Helicolithus trabeculatus (Górka) Verbeek
R
R
Isocrystallithus sp.
?
Lithraphidites acutus Thierstein
R
R
Lithraphidites carniolensis Deflandre
R
R
R
R
R
Manivitella pemmatoidea (Deflandre) Thierstein
F
F
C
F
F
F
C
F
Micrantholithus hoschulzii (Reinhardt) Thierstein
r
Micrantholithus obtusus Stradner
r
Nannoconus steinmanii Kamptner
r
Perissocyclus fenestratus (Stover) Black
R
Prediscosphaera columnata (Stover) Perch-Nielsen
R
F
R
F
F
F
F
Prediscosphaera cretacea (Arkhangelsky) Gartner
R
F
R
Prediscosphaera ponticula (Bukry) Perch-Nielsen
F
C
R
F
Prediscosphaera spinosa (Bramlette et Martini) Gartner
R
Prediscosphaera sp. (spines)
R
F
Polypodorhabdus madingleyensis Black
R
Radiolithus hollandicus Varol
F
F
F
R
Retacapsa angustiforata Black
R
R
R
F
Retacapsa crenulata (Bramlette et Martini) Grün
R
R
R
R
R
Retacapsa surrirela (Deflandre et Fert) Grün
R
Retacapsa sp.
F
R
Rhagodiscus angustus (Stradner) Reinhardt
F
R
R
R
F
Rhagodiscus asper (Stradner) Reinhardt
R
Rotelapillus crenulatus (Stover) Perch-Nielsen
R
Seribiscutum primitivum (Thierstein) Filewicz et al.
F
Speetonia colligata Black
r
Staurolithites sp.
R
Staurolithites crux (Deflandre et Fert) Caratini
R
Stradneria sp.
R
Tegumentum stradneri Thierstein
R
R
R
R
Tranolirthus gabalus Stover
R
C
Tranolithus orionatus (Reinhardt) Reinhardt
R
R
R
C
Tubodiscus sp.
r
Watznaueria barnesae (Black) Perch-Nielsen
A
C
A
A
A
A
A
A
Watznaueria biporta Bukry
R
R
F
F
F
F
Watznaueria britannica (Stradner) Reinhardt
F
R
F
R
R
R
R
Watznaueria fossacincta (Black) Bown
R
Zeugrhabdotus bicrescenticus (Stover) Burnett
R
R
R
F
Zeugrhabdotus diplogrammus (Deflandre) Burnett
F
F
F
C
F
F
C
Zeugrhabdotus embergerii (Noël) Perch-Nielsen
R
R
F
F
R
F
F
Zeugrhabdotus erectus (Deflandre) Reinhardt
F
Zeugrhabdotus noeliae Rood et al.
F
C
F
R
C
Zeugrhabdotus scutula (Bergen) Rutledge et Bown
F
F
R
Zeugrhabdotus xenotus (Stover) Burnett
R
384 SVOBODOVÁ, HRADECKÁ, SKUPIEN and VÁBENICKÁ
Rotalipora reicheli corresponds to the Middle Cenomanian in-
terval. The nannofossils are characterized by joint occurrence
of Corrolithion kennedyi and Lithraphidites acutus and it is
correlated with the UC3-UC4 Zone of the Middle?Upper
Cenomanian.
Sample 2/VIII
The occurrence of the species Rotalipora cushmani
(Rotalipora cushmani Zone) corresponds to the upper part of
the Middle Cenomanian to Upper Cenomanian. The poor as-
semblage of angiosperm pollen grains (mainly Tricolpites
sagax and the absence of the Upper Cenomanian angiosperm
pollen from the Normapolles group) corresponds to Lower
Middle Cenomanian.
Note: The dinoflagellate cysts are interpreted as the upper-
most Albian. The poor nannofossil assemblage is character-
ized by Prediscosphaera cretacea and Gartnerago theta and
by the absence of younger Cenomanian species and so it can
be correlated with the lowermost Cenomanian.
Paleoenvironmental interpretation
The spore and pollen assemblages of samples 15/V and
49C/VIII are also characterized by the presence of non-ma-
rine aquatic palynomorphs Lecaniella sp. and Tetraporina
sp., which are found in the fluvio-lacustrine environment.
Some prasinophytes such as Pterospermella australiensis,
acritarchs Veryhachium rhomboidium, and faunal remains
chitinous foraminiferal linings (planispiral, trochospiral,
biserial types) were found especially in sample 49C/VIII.
Scolecodonts were recorded in sample 15/V and 49C/VIII.
Some palynologists such as Jarvis et al. (1988) and Courtinat
et al. (1990) agree that co-occurrence of chitinous foraminifers
and scolecodonts may indicate environments with low oxygen
content. The presence of gymnosperm taxa Taxodiaceae-
pollenites, Corollina/Classopollis and some thick-walled
spores from Camarozonosporites, Cicatricosisporites, Appen-
dicisporites, Corniculatisporites, or Gleicheniidites carinatus
indicates the xerophytic character of the flora.
Fig. 18. Distribution of selected index microfossil species from samples of tramberk, Kotouè Quarry. Foraminiferal zones: Rotal. reich.
Rotalipora reicheli, Rotal. cushm. Rotalipora cushmani.
Marine biostratigraphy
Non-marine biostratigraphy
Sample
No.
Lithology
Age
Fo
ra
m
ini
-
fe
ra
l zo
ne
s
N
anno
-
pl
ank
ton
zon
es
Dinoflagellate
cysts
Angiosperm
pollen grains
2/VIII
grey
claystone
Upp
er
Ro
ta
l.
cu
sh
m
.
Kiokansium unituberculatum,
Litosphaeridium siphoniphorum
rare tricolpate pollen
Tricolpites sagax
1/VIII
greenish
marlstone
29/IV
green-grey
sandy claystone
UC
3
UC4
30/IV
green-grey
clayey siltstone
Ro
ta
lip
or
a
reich
eli
negative
negative
49C/VIII
dark grey
claystone
Mi
dd
le
?
Ro
ta
l.
reich.
UC
1
?U
C3
Epelidosphaeridia spinosa,
Litosphaeridium arundum,
L. siphoniphorum
Psilatricolporites sp.
Brenneripollis peroreticulatus
Liliacidites dividuus
0/VIII
greenish
marlstone
UC0c
negative
negative
15/V
sandy
siltstone
C E
N
O
M
A
N
I A
N
Lo
w
er
neg.
Tricolpites sagax, T. variabilis,
Psilatricolporites sp.
49B/VIII
black
claystone
b
Ovoidinium verrucosum
Protoellipsodinium
spinocristatum
Palaeohystrichophora
infusorioides
Litosphaeridium siphoniphorum
11/VI
grey
claystone
AL
B
IA
N
Upp
er
BC
27
/U
C0
a
b
negative
negative
MICROFOSSILS OF THE SHALES FROM TRAMBERK (OUTER WESTERN CARPATHIANS) 385
Fig. 19. Paleoenvironmental interpretation of main changes in marine environment during the AlbianCenomanian in Kotouè Quarry
based on foraminifers, dinocysts and scolecodonts.
The dinoflagellate cyst assemblages are dominated by
dinocysts characterizing deep neritic sea (e.g. Oligosphae-
ridium, Spiniferites), but oceanic types (Pterodinium
cingulatum, Lister & Batten 1988, Leereveld 1995) are also
frequent in sample 2/VIII and 49C/VIII. A part of the as-
semblage is formed by dinocysts redeposited from shallow
marginal parts of the sedimentary space (presence of brackish
Odontochitina and littoral Circulodinium species). The di-
noflagellate assemblage in sample 15/V differs markedly in
the prevalence of representatives of the genus Ovoidinum. The
composition of the dinoflagellate assemblages of samples 15/
V and 49B/VIII corresponds to shallow neritic sea. No oceanic
dinocyst types appear. Littoral (Circulodinium, Systemato-
phora) and inner neritic (Cribroperidinum) specimens are fre-
quent.
The character of foraminiferal assemblages of the studied
samples and their basic characteristics suggest marine sedi-
mentation within neritic to inner shelf environments. Poor
foraminiferal assemblages were found in samples 15/V and
2/VIII. Only eight species were found in sample 15/V and
no agglutinated foraminifers were present in sample 2/VIII.
In these two samples, each species was represented only by
one or two specimens with the exception of planktonic
Globigerinelloides ultramicra (Subbotina) and Hedbergella
delrioensis (Carsey) in sample 2/VIII. A few species of cal-
careous benthos (genera Lingulogavelinella, Lenticulina,
Neobulimina and Praebulimina), which represent epifaunal to
shallow infaunal deposit feeders (Koutsoukos & Hart 1990),
were found in these samples. Agglutinated Textularia foeda
Reuss was found only in sample 15/V and was absent in
other studied samples. It is possible to speculate on the basis
of the poor assemblage with sporadic presence of genus
Lingulogavelinella, which tolerates low-oxygen conditions,
that the foraminifers were probably living in a dysaerobic en-
vironment. Representatives of the gavelinellids (L. globosa, L.
jarzevae, L. pazdroae) were frequent in samples 0/VIII and
11/VI. Their assemblages are representative for inner shelf
associations. A similar foraminiferal assemblage has been also
found in the Cenomanian sediments of the Bohemian Creta-
ceous Basin (Ulièný et al. 1993; Hradecká 1996). Foramini-
feral assemblages from rather deeper neritic biotopes were
found in samples 29/IV and 30/IV (Middle Cenomanian).
Representatives of low to high conical morphotypes of genera
Trocholina and Turrispirillina prevail, together with
Marssonella oxycona (Reuss). Plankton is represented by rare
occurrences of Hedbergella delrioensis (Carsey), Rotalipora
greenhornensis (Morrow) and Rotalipora reicheli Mornod.
Fragments of echinoderm spines, cyclostomate bryozoans and
fish teeth were also found in both samples. Rotalipora is fre-
quent in sample 1/VIII. The relatively rich foraminiferal as-
semblage of this sample represents a deeper-water environ-
ment (middle to outer neritic and maybe deeper). The deepest
Sample No.
Lithology
Age
Paleoenvironmental interpretation
2/VIII
grey
claystone
Up
pe
r
prevalence of calcareous foraminifers
planktonic foraminifers with keeled tests
deep neritic and oceanic dinocyst types
1/VIII
greenish
marlstone
29/IV
green-grey
sandy claystone
30/IV
green-grey
claeye siltstone
49C/VIII
dark grey
claystone
Mi
dd
le
deep
neritic
sea
abundance of calcareous nannofossils
keeled planktonic foraminifers;
agglutinated and calcareous conical morphotypes
of benthos
deep neritic and oceanic dinocyst types
abundance of calcareous nannofossils
0/VIII
greenish
marlstone
15/V
sandy
siltstone
C
E
N
O
M A
N
I
A
N
Low
er
49B/VIII
black
claystone
11/VI
grey
claystone
AL
B
IA
N
Up
pe
r
shallow
dysaerob.
conditions
neritic
sea
group of gavelinellids frequent
foraminifers toleranting low oxygen conditions (Lingulogavelinella) and
scolecodonts; absence of calcareous nannofossils
group of gavelinellids frequent
386 SVOBODOVÁ, HRADECKÁ, SKUPIEN and VÁBENICKÁ
biotope is also represented by agglutinated genera Ammo-
baculites, Ammodiscus and Arenobulimina. Specimens of the
genus Lingulogavelinella were not found here.
Both the poor state of preservation and the low quantity of
calcareous foraminifers and nannofossils reflect the paleo-
environmental, depositional and post-depositional conditions.
The presence of calcareous nannofossils and microfauna indi-
cates sea of normal salinity and depositional conditions above
the carbonate compensation depth (CCD). Strong carbonate
dissolution of probably post-mortem tests is supported by the
following calcareous nannofossil phenomena: 1. high num-
bers of the genus Watznaueria, 2. destroyed central areas of
placoliths (such as in genera Axopodorhabdus, Eiffellithus or
Prediscosphaera), 3. a very low number or absence of
nannofossils formed by subtle specimens, such as genera
Corrolithion or Rotelapillus. According to Roth & Krumbach
(1986), the positive correlation of organic carbon content of
sediment and the relative abundance of W. barnesae are in-
dicative of the carbonate dissolution caused by the release of
carbon dioxide during the oxidation of organic matter.
A brief overview of the main phenomena and their
paleoenvironmental interpretations were compiled into a table
(Fig. 19). A shallow neritic environment with a short interval
of low-salinity and dysoxic conditions is documented in the
uppermost Albian and Lower Cenomanian deposition. Deep-
ening of the sedimentary basin is evident during the
Cenomanian. These data correspond to the paleogeographical
reconstruction of the Outer Group of nappes of the Western
Carpathians. According to Stráník et al. (1996), the Silesian
Unit is the external sedimentary area of the northern part of
Tethys, which was probably situated on the southeastern pas-
sive margin of the European Platform.
Note: An interesting feature was observed during the study
of palynomorph residue (sample 49C/VIII) using the scan-
ning electron microscope a relatively high number of cal-
careous nannofossils was found in the palynomorph residue
after strong maceration techniques. This surprising phenom-
enon can be explained by the fact that calcareous nannofossils
were probably mineralized by other elements which protected
them from aggressive acids during the laboratory maceration
Fig. 20. Pollen grains, dinoflagellate cysts, and calcareous nannofossils. Figs. 19 tramberk sample 49C/VIII (SEM micrographs). 1
Clavatipollenites sp. 2 Achomosphaera neptuni (Eisenack, 1958) Davey et Williams, 1966. 3 Litosphaeridium siphoniphorum (Cook-
son et Eisenack, 1958) Davey et Williams, 1966. 4 Pervosphaeridium pseudhystrichodinium (Deflandre, 1937) Yun, 1981. 5 Palaeo-
hystrichophora infusorioides Deflandre, 1935. 6 dinoflagellate cyst Spiniferites sp. and inside nannofossil Eprolithus floralis (Stradner)
Stover. 7 Prediscosphaera columnata (Stover) Perch-Nielsen. 8 left: Prediscosphaera cretacea (Archangelsky) Gartner; right:
Manivitella pemmatoidea (Deflandre) Thierstein. 9 Watznaueria sp. (coccosphere).
MICROFOSSILS OF THE SHALES FROM TRAMBERK (OUTER WESTERN CARPATHIANS) 387
techniques (see Methods and Fig. 20. 6-9). Alternatively, they
could have been covered by organic matter secondarily lining
calcareous plates of coccoliths.
Conclusions
The sporomorphs, dinoflagellate cysts, foraminifers and
calcareous nannofossils recovered from dark grey and light
greenish pelitic fills in the limestone body of the tramberk
Member allowed their assignment to the Upper AlbianUpper
Cenomanian.
Dark organic-rich sediments contain mainly
palynomorphs, while light greenish highly calcareous sedi-
ments provided higher numbers of foraminifers and calcareous
nannofossils.
Mixing of Boreal and Tethyan elements in sporomorph
and foraminifera assemblages was identified in the tramberk
area during the Early Cenomanian (the foraminiferal genus
Rotalipora represents the Tethyan Realm, the Boreal elements
are Gaudryina, Dorothia, Gyroidinoides, the sporomorphs
characteristic for Tethyan realm are pteridophyte spores,
Collarisporis fuscus and Corniculatisporites auritus).
The dinoflagellate cyst assemblages from the tramberk
area confirmed the latest AlbianCenomanian age of the
pelitic fills and are correlable with the other parts of the
Silesian Unit. The quantitative composition of dinocysts re-
flects open-sea conditions.
Two planktonic zones were determined: Rotalipora
reicheli Zone (Middle Cenomanian) (samples 1/VIII, 29/
IV, 30/IV, 49C/VIII) and Rotalipora cushmani Zone (Up-
per Cenomanian) (sample 2/VIII). The foraminiferal assem-
blages from samples 0/VIII, 11/VI, 15/V, 49B/VIII be-
long to zones with the stratigraphical range from Rotalipora
appenninica to Rotalipora cushmani (Upper Albian
Cenomanian). Calcareous benthos prevails, agglutinated
benthos is less frequent and plankton occurs occasionally.
The presence of calcareous nannofossils and calcareous
microfauna indicates the depositional conditions above the
CCD. Strong post-mortem carbonate dissolution is docu-
mented by high numbers of genus Watznaueria, and by the
low numbers or absence of nannofossils formed by subtle
specimens.
Gavelinellids, dinocysts and poor nannofossil assem-
blages document inner shelf and shallow neritic sea in the Up-
per Albian. A short interval of dysaerobic conditions is
marked by the occurrence of foraminifers tolerating low oxy-
gen conditions and by scolecodonts. The deepening of the
sedimentary basin during the Cenomanian is supported by
higher numbers of calcareous foraminifers and nannofossils.
Acknowledgments: This study is a contribution to the project
Microfossils from the Lower Cretaceous pelitic sediments in
the tramberk area (Outer Western Carpathians): biostratigra-
phy, paleoecology (Grant No. 205/01/1582), supported by
the Grant Agency of the Czech Republic. The authors thank
Ing. A. Langrová, Ing. V. Böhmová, and RNDr. Z. Korbelová,
Institute of Geology AS CR for CAMECA micrographs
(palynomorphs and nannofossils) and Ing. A. Gabaová,
Czech Geological Survey (foraminifers). Suggestions of the
reviewers Dr. M. C. Melinte (Bucharest), Dr. Z. Stráník
(Brno), Dr. J. Soták (Bratislava), but above all Dr. P. Gedl
(Kraków) helped to improve the manuscript. We wish to thank
Ing. L. Staek, Ing. Stoèek and Ing. J. Monsport from the
Kotouè tramberk Company Ltd. for the possibility to collect
samples in the Kotouè Quarry.
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