www.geologicacarpathica.com
GEOLOGICA CARPATHICA
, JUNE 2016, 67, 3, 239–256
doi: 10.1515/geoca-2016-0016
Upper Cretaceous to Lower Miocene of the Subsilesian Unit
(Western Carpathians, Czech Republic):
stratotypes of formations revised.
MIROSLAV BUBÍK
1
, JURAJ FRANCŮ
1
, HELENA GILÍKOVÁ
1
, JIŘÍ OTAVA
1
and LILIAN ŠVÁBENICKÁ
2
1
Czech Geological Survey, Leitnerova 22, 602 00 Brno, Czech Republic;
miroslav.bubik@geology.cz, juraj.francu@geology.cz, helena.gilikova@geology.cz, jiri.otava@geology.cz
2
Czech Geological Survey, Klárov 131/3, 118 21 Praha, Czech Republic; lilian.svabenicka@geology.cz
(Manuscript received June 11, 2015; accepted in revised form March 10, 2016)
Abstract: Type sections/areas for all four formations distinguished in the sedimentary succession of the Subsilesian
Unit on Czech territory were revisited and described. New data on lithology, sedimentology, fossil record, biostratigraphy,
heavy-minerals and geochemical proxies are based on observations and analysis of these sections. The historical type
section of the Frýdek Formation was destroyed during railway construction in 19
th
century. Outcrops of Campanian to
Maastrichtian marls and sandstones on the southwestern slope of “Castle hill” at Frýdek, are proposed as a new type
section. The Ostravice riverbed in Frýdlant nad Ostravicí was originally designated as the type area, not mentioning
the particular section. This area, even when supplemented with Sibudov Creek, does not show all typical facies of
the formation. The outcrops range from lowermost Eocene to Eocene–Oligocene transition. In the original description
of the Menilite Formation Glocker mentioned several localities in the area covering the Ždánice, Subsilesian and
Silesian units, not mentioning the principal one. The single sections, each not exceeding a thickness of 2 m, are not
sufficient to be a type section. Instead of that, we propose the area between Paršovice and Bystřice pod Hostýnem,
covering the historical localities, as the type area. The type locality of the Ženklava Formation is an outcrop in an unnamed
creek in Ženklava according to the original definition. It seems to be reasonable to extend the type section to the whole
500 m long section of the creek with the outcrops that better illustrate the lithological variability of the formation. New
biostratigraphic data allow assignment to late Egerian (Eggenburgian?).
Key words: Subsilesian Unit, Outer Flysch Carpathians, Cretaceous, Palaeogene, Miocene, lithostratigraphy, biostratigraphy,
heavy minerals, geochemistry.
Introduction
Geological studies of the Outer Flysch Carpathians in
northern Moravia and Silesia started around the middle of
the 19
th
Century. Generations of geologists accumulated
a huge complex of knowledge. The delimitation of the Sub-
silesian Unit as a distinct nappe was done relatively late in
connection with the development of micropalaeontology and
biostratigraphy after the Second World War (Książkiewicz
1951; Hanzlíková et al. 1953). Formal lithostratigraphic sub-
division of the sedimentary succession in the studied area
into four formations was finished by Eliáš (1993, 1998). This
complex of knowledge, nevertheless, contains a number of
inadequate definitions and synonyms that caused further
confusion. Inadequate description and confusion about the
type locality led to the question of what actually is the Žen-
klava Formation. If we are correct, no attempt has been made
since Glocker’s geological studies in 1843 to choose a defi-
nite type locality from seven localities mentioned in the
original paper. Finally, neither a detailed description, nor de-
tails of the position of the type sections for the Frýdek and
Frýdlant formations have been published since these forma-
tions were described. These problems still need to be fixed
for the sake of a definite and stable lithostratigraphy.
Type sections are an essential clue in the case of any doubt
about the nature and position of a lithostratigraphic unit. Any
revision or redefinition of units has to be based on study of
the type section that serves as the standard documenting the
true nature of the unit erected by the original author.
In today’s open Europe the borderlines play a much smaller
role then in the past. It is no longer acceptable that geological
units stop at these borders just because of the isolation and
traditionalism of national geological communities. Projects
of European geological maps will demand more correlation
and unification and the type sections may be needed for such
a task.
The main objective of this paper is to provide adequate
description of the type sections for all four valid formations
of the Subsilesian Unit in its western sector (Moravo-Silesian
Beskydy and its foothills) and select one type section from
several original localities where needed.
Geological setting
The Subsilesian Unit is a part of the Outer Group of
Nappes of the Outer Flysch Carpathians. It is exposed in
a zone along the margin of the Outer Flysch Carpathians and
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GEOLOGICA CARPATHICA
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also in several tectonic windows within the Silesian Nappe
(Fig. 1). The zone runs for a distance of about 100 km from
the vicinity of Kelč in Moravia to the vicinity of Bielsko-
Biała in Poland (Eliáš 1998). In the broader concept of
Polish authors the unit extends even much further to the
Eastern Carpathians with possible equivalents in Ukraine
(Ślączka et al. 2006). Eliáš (1998) compared this eastern sec-
tor of the Subsilesian Unit with the Kelč facies of the Sile-
sian Unit. He interpreted the western continuation of the
Subsilesian Unit as a part of the Eastern Alpine Helveticum.
Roth and Hanzlíková (1967) unified the Ždánice Unit and
Waschbergzone in the South with the Subsilesian Unit in the
North under the term “Ždánice-Subsilesian Unit”. They ar-
gued with uniform facies development during the Late Creta-
ceous–Eocene. The Subsilesian Unit can still be understood
as a distinct tectonic unit based on its specific structural fea-
tures. Intense compression and the load of the robust and
competent overlying Silesian Nappe deformed the sediments
much more intensively compared with the same sediments in
the Ždánice sector, outside the influence of the Silesian
Nappe. The pelitic formations of the Subsilesian Nappe
possess complicated structure with frequent tectonic slices,
lenses, flat overturned folds and zones of tectonic breccia
(Roth 1971; Menčík et al. 1983). The complexity of defor-
mation increases at the base of the nappe. The upper part of
the nappe includes slices of the overlying Silesian Unit.
The sedimentary succession of the Subsilesian Unit in
Czech territory is subdivided into four formations: the Frý-
dek, Fýdlant, Menilite and Ženklava fms. (see Fig. 2).
In Polish teritory the subdivision into formations was pro-
posed by Olszewska (1997) on the basis of an unpublished
lithostratigraphy elaborated by the working group of
A. Wójcik for the general map of Poland. They distinguish
(from base): Frýdek Fm., Węglówka Fm., Bachórz Fm.
(=“Hieroglyphic Beds”), Znamirowice Fm. (=”Globigerina
Marls”), and Rudawka Rymanowska Fm. (=Menilite Fm.).
These formations are not widely accepted and various au-
thors distinguish numerous informal units not assigned to
any formation (e.g. Waśkowska 2011; Cieszkowski et al.
2012).
The sedimentary succession of the unit was deposited on
the northern slope of the Silesian Basin and on the Subsile-
sian Ridge (Golonka 2011). Particularly the grey marls and
siltstones of the Frýdek Formation in the western sector of
the Subsilesian Unit represent typical slope facies. Red and
variegated marls of Węglówka type were deposited under
oligotrophic conditions and low sedimentary rates what indi-
cate the setting of a submarine elevation (Subsilesian Ridge).
Material
Biostratigraphical, petrographical, mineralogical and
geochemical data mentioned in description of the type sec-
tions are based mostly on newly collected rock samples. The
small reference samples (rock pieces) are stored at sample
depository of the Czech Geological Survey in Brno. Micro-
palaeontological residues, picked microfossils, thin sections
and heavy mineral samples are stored in the same place.
Field observations including description of exposures, litho-
logy, structures, GPS position, and photodocumentation are
recorded in the documentation database of the CGS.
Fig. 1. Overview tectonic map with situation of type sections and
areas in the Subsilesian Unit in Moravia.
Fig. 2. Lithostratigraphic chart with stratigraphic ranges of studied
sections.
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STRATOTYPES OF U. CRETACEOUS–L. MIOCENE FORMATIONS (W CARPATHIANS)
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Methods
During the field observations the most complete sections
were measured and described bed-by-bed. GPS position of
sections was recorded using Garmin 60CSx (Table 1). The
geological layer in the situation maps is based on the on-line
geological map 1:50,000 of the Czech Geological Survey
(www.geology.cz) but modified according to new field ob-
servations. The samples for microfossils were disintegrated
in solution of sodium bicarbonate and washed on sieves of
mesh size 0.063 mm. Microfossils from hard carbonate rocks
were retrieved by an acetolysis using 80 % acetic acid fol-
lowing Lirer (2000). Microfossils were manually picked under
binocular microscope. Smear slides for calcareous nannofos-
sils were prepared using a decantation method (Švábenická
2012). Nannofossil data were correlated applying Upper
Cretaceous UC (Burnett 1998) and Palaeogene NP (Martini
1971) and NNT (Varol 1998) nannoplankton zones.
Photodocumentation of microfossils was done using an SEM
microscope Jeol JSM-6380 microscope Nikon SMZ1500
equipped with camera ProgResCT3. Nannofossils were ob-
served and documented using a Nikon Microphot-FXA
transmitting light microscope. For study of heavy minerals
the psammitic rocks were crushed and the size fraction
0.063–0.25 mm washed on sieves. Heavy minerals were sepa-
rated from the sieved fraction using tetrabromethane
(C
2
H
2
Br
4
). When needed, opaque magnetic minerals were
removed using a magnetic separator. The translucent heavy
minerals were quantitatively analysed from counts between
200 and 1200 grains. The recorded % value reflects a grain
number. The ZTR maturity index expresses total percentual
quantity of zircon, tourmaline and rutile grains in the associa-
tion. The index increases with both chemical and mechanical
maturity of the psammitic fraction. Total inorganic carbon,
total organic carbon and total sulphur (TIC, TOC and TS)
were analysed using the ELTRA elementar analyser. Nanno-
fossil slides, thin sections and heavy mineral fractions were
prepared at the CGS laboratory in Prague. Processing of fora-
minifer samples and geochemical analysis were done at the
CGS laboratory in Brno.
Frýdek Formation
History of studies
Hochstetter (1852) was the first to study the geology of the
outcrop on the right bank of the Ostravice River below the
Frýdek castle/chateau. Based on this outcrop he introduced
a new stratigraphic unit “Friedek-Mergel” or “Friedek
Schichten”, now classified as the Frýdek Formation. Origi-
nally he characterized the strata as
20 to 30 feet thick ash grey marls,
sandy in places, containing fine
mica, frequent calcite veins, pyrite
nodules and small gypsum crystals
covering crack surfaces. At the base
of the outcrop he reported a one-foot
thick bank of calcareous sandy con-
glomerate composed of quartz
grains, mica and coal fragments.
Hochstetter (l.c.) also reported in de-
tail finds of Baculites ammonite fau-
na within the marls. Based on these
finds Hohenegger (1852) assigned
the “Baculiten-Schichten” to the
Gault and later (1861) correlated
them with the “Plänermergel” (Tu-
ronian–Coniacian) of the Bohemian
Cretaceous Basin. Finally Liebus
and Uhlig (1902) produced a sys-
tematic description of the ammo-
nites and recognized the “upper
Senonian” age of this fauna.
Růžička and Beneš (1949) conducted
the first micropalaeontological in-
vestigations and reported rich Upper
Cretaceous foraminifer fauna. Eliáš
and Hanzlíková (1964) informed
about the results of petrographical
and microbiostratigraphical study.
Based on planktonic foraminifers,
they assigned the strata at “Castle
hill” to the Maastrichtian. Systematic
study of foraminifers was done by
Table 1: Overview of the studied sections and their GPS position.
locality
section/
point
map
sheet
latitude-longitude
formation
beginning
end
Frýdek
MB001
25-221
N49 41 05.0 E18 20 46.2
N49 41 03.1 E18 20 49.9
Frýdek Fm.
MB026
25-221
N49 41 09.4 E18 20 34.8
N49 41 08.4 E18 20 37.9
Frýdlant n.
O.
MB006
25-223
N49 35 03.3 E18 21 55.9
Frýdlant
Fm.
MB007
25-223
N49 35 07.3 E18 21 55.7
N49 35 04.9 E18 21 55.7
MB008
25-223
N49 35 11.4 E18 21 54.9
N49 35 10.1 E18 21 55.5
MB009
25-223
N49 35 19.5 E18 21 56.5
N49 35 18.0 E18 21 55.7
MB010
25-223
N49 35 29.0 E18 21 58.1
N49 35 24.3 E18 21 55.9
MB021
25-223
N49 34 39.2 E18 22 02.8
MB022
25-223
N49 34 41.4 E18 22 01.6
MB023
25-223
N49 34 41.4 E18 22 01.6
MB024
25-223
N49 35 16.3 E18 21 57.9
N49 35 14.3 E18 21 58.5
Sibudov
MB011
25-223
N49 34 51.0 E18 22 48.5
N49 34 51.1 E18 22 49.6
MB012
25-223
N49 34 49.3 E18 22 43.1
N49 34 50.5 E18 22 43.2
MB013
25-223
N49 34 46.4 E18 22 25.1
MB014
25-223
N49 34 45.0 E18 22 16.7
N49 34 44.4 E18 22 17.3
Dolní
Těšice
MB032
25-141
N49 29 34.1 E17 48 04.1
Menilite
Fm.
MB033
25-141
N49 29 16.3 E17 47 58.9
Rakov
MB034
25-141
N49 29 09.0 E17 42 22.6
MB035
25-141
N49 29 03.6 E17 42 30.3
MB036
25-141
N49 29 04.6 E17 42 45.7
MB037
25-141
N49 29 02.7 E17 42 52.3
MB038
25-141
N49 29 19.4 E17 43 05.2
MB039
25-141
N49 29 11.9 E17 43 05.9
MB040
25-141
N49 29 04.7 E17 42 24.0
Paršovice
MB041
25-141
N49 30 10.0 E17 42 18.4
N49 30 10.1 E17 42 19.4
Sovadina
MB001
25-134
N49 25 12.0 E17 39 26.0
MB002
25-134
N49 25 19.2 E17 39 28.7
Horní
Těšice
MB043
25-141
N49 29 29.6 E17 47 42.7
N49 29 29.3 E17 47 41.8
MB044
25-141
N49 29 32.6 E17 47 33.0
N49 29 32.2 E17 47 33.1
MB046
25-141
N49 29 26.4 E17 47 42.6
Ženklava
MB046
25-213
N49 33 44.8 E18 06 03.1
N49 33 44.5 E18 06 09.2
Ženklava
Fm.
MB047
25-213
N49 33 44.9 E18 06 09.7
N49 33 45.5 E18 06 11.7
MB048
25-213
N49 33 46.2 E18 06 13.1
MB049
25-213
N49 33 46.3 E18 06 16.9
MB050
25-213
N49 33 46.8 E18 06 19.8
MB051
25-213
N49 33 46.7 E18 06 22.8
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Hanzlíková (1969 and 1972), later supplemented with evalua-
tion of calcareous nannofossils (Hanzlíková et al. 1982).
Description of outcrops
The south-western steep slope of the “Castle hill” in Frý-
dek has outcrops at two locations (Fig. S1 in the Supplemen-
tary Material file): below Hasičská street (section MB001)
and below an orchard (section MB026). The slope is covered
by dense growth of bush and trees.
MB001. At the present time, claystones and sandstones
crop out in a few small flat isolated outcrops (Fig. 3A) over
a distance of 96 m. Brown grey silty marls prevail over sand-
stones. The grey laminated fine-grained calcareous sand-
stones occur in banks up to 1 m thick. Locally, sandstone
banks are deformed by gravity folds. The measured bedding
dip indicates fold deformation (280/35°, 313/48°, 152/65°).
MB026. The isolated exposures are situated in a steep up-
per part of a railway cut below the old orchard over a dis-
tance of 70 m. At the north-western end of the cut, slope
debris of coarse-grained biodetritic sandstone was observed.
The largest exposure in the middle part of the cut represents
an 8.5 m thick continuous section (Fig. S2 in the Supplemen-
tary Material file). Brown grey silty marls prevail over the
grey marls and isolated banks of grey calcareous sandstone.
Some sandstone banks are deformed to gravity folds
(Fig. 3B).
Lithology and sedimentology
Grey brown calcareous silty marls are the prevailing rock
type in the outcrops. Brownish grey weathered fine- to me-
dium-grained calcareous sandstones occur in isolated banks
10 to 100 cm thick (Fig. 4). According Eliáš and Hanzlíková
(1964) claystones comprise 50–
60 % of silt and 5–10 % of sand.
Greywacky sandstones comprise
30–45 % of calcite, 20–30 % of
clay matrix, 25–45 % of subangu-
lar quartz, 1–2 % of feldspars,
1–2 % of bioclasts, 1 % of clayey
clasts and accessoric muscovite,
biotite, chlorite, pyrite, glauconite,
siderite and dolomite.
Fine-grained calcareous sand-
stone to sandy limestone
(MB001Z4) shows in thin section
carbonate basal cement, that cor-
rodes clastic grains. Silicification
is observed in places. Well-sorted
clasts comprise monocrystallic
and aggregate grains of quartz
(dominant), bioclasts (about
10 mod. %: mainly small calca-
reous benthic foraminifera, calci-
fied sponge spicules, inoceramid
prisms and phytodetrite), K-feld-
spar and plagioclase (20 mod. %),
glauconite (3–5 mod. %), musco-
vite, biotite and chlorite
(1 mod. %). Plagioclases prevail
over K-feldspars. They used to be
both sericitized.
Coarse-grained calcareous
sandstone to sandy limestone
(sample MB026A2; Fig. 5) has
carbonate basal cement corroding
clastic grains. The clastic compo-
nent comprises sub-oval to sub-
angular grains of monocrystallic
and aggregate of quartz ranging
between 0.5 and 0.75 mm
(dominant), K-feldspar and pla-
gioclase (20 mod. %), bioclasts
(20 mod. %: mainly bryozoans,
coralline algae, echinoid spines,
small calcareous benthic fora-
Fig. 3. Outcrops of the Frýdek Formation at Frýdek: A — calcareous sandstone at the type section
(MB001), photograph: M. Bubík, 2012; B — Gravity fold consisting of calcareous sandstone be-
low an orchard (MB026), photograph: M. Bubík, 2014.
Fig. 4. Lithology and sedimentology of the MB026 Frýdek below an orchard with samples indi-
cated by asterisk.
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minifera and plant debris), sub-oval pebbles of gneisses and
mica schists (7 mod. %), muscovite, biotite, chloritized
biotite and chlorite (5 mod. %), glauconite (2–3 mod. %) and
rarely lithoclasts of carbonatized volcanite, granitoids and
quartzites.
The sandstones represent turbidites with wavy lamination,
ripple marks and burrowings. Silty marls with positive gra-
dation were probably also deposited from turbidite currents.
Gravity folds indicate high sedimentary rate and submarine
slope failures that may locally disturb the stratigraphic order
of strata. Hemipelagic sedimentation is indicated by the pre-
sence of deep-sea agglutinated foraminifer fauna (Saccorhiza,
Bathysiphon, Arthrodendron) in the terminal part of graded
marl rhythms.
Fossil record and biostratigraphy
Hohenegger (1861) reported from the type locality a mol-
lusc fauna with Baculites faujasi Lam., Belemnites lanceola
tus Sow., Turrilites cf. undulatus Sow., Pinna nodulosa
Reuss and
Inoceramus latus Mant. and compared it with the
Turonian–Coniacian fauna of the Bohemian Cretaceous Ba-
sin. Based on revision of an old collection from Frýdek, Lie-
bus and Uhlig (1902) described stratigraphically important
ammonites Baculites hochstetteri Liebus and Puzosia aff.
planulata Sow. indicating upper Senonian age. No ammo-
nite finds have been reported since these times. Marls of the
Frýdek Formation contain rich foraminiferal taphocoenosis.
Hanzlíková (1969) assigned the Frýdek Formation based on
the finds of Abathomphalus mayaroensis from test trenches
on the slope of the Castle hill to the upper Maastrichtian.
Later revision of biostratigraphy supplemented by calcareous
nannofossils revealed that the main part of the section is lo-
wer Maastrichtian (Hanzlíková et al. 1982). The authors con-
sidered that the finds of Abathomphalus mayaroensis at the
base of the section could come from another tectonic slice.
Newly collected micropalaeontological samples gave
taphocoenosis dominated by small planktonic foraminifera
Fig. 5. Thin section of coarse-grained biodetritic sandstone with
calcareous algae, bryozoans and benthic foraminifer Gyroidinoides
sp. (sample Frýdek MB026A2).
(Heterohelix, Macroglobigerinelloides and Rugoglobigerina).
Benthic foraminifera are represented by tiny calcareous taxa:
Quinqueloculina sp., Buchnerina sp., Patellina sp., Cribro
conica sp., Praebulimina reussi, P. triangularis, Eouvigerina
serrata, Globimorphina sp., Pyramidina cimbrica, Alabamina
dorsoplana, Rotorbinella supracretacea, Pullenia marssoni,
Pararotalia cf. bandyi, Gyroidinoides spp., Gavelinella spp.
etc. accompanied by scarce agglutinated forms
Spiroplectammina spp. Sample MB001Z3). The coarser size
fraction of residues contains usually robust forms of benthos
like Lenticulina cf. discrepans, Nodosaria spp., Siphono
dosaria spp., Hemirobulina hamuloides, Praebulimina
petroleana, Allomorphina obliqua, Nuttallinella florealis,
Remesella varians and keeled plankton Globotruncana spp.
Claystones from the top of graded rhythms (samples MB026
B3, B4, B5) contained abundant large agglutinated taxa
Saccorhiza sp., Bathysiphon spp. and Arthrodendron sp.
Preliminary results of planktonic foraminifer study does not
allow biostratigraphical subdivision within the upper Cam-
panian–Maastrichtian interval.
The foraminifer fauna is accompanied by abundant calcite
prisms from destroyed inoceramid shells. Less common are
sponge spicules, calcispheres, coalified plant debris (tissues,
seeds, and cuticles), echinoid elements and ostracods. Rarely
calcified radiolarians and pyritized planktonic diatoms occur.
Newly studied calcareous nannofossils enable us to distin-
guish three stratigraphic levels:
1) upper Campanian UC15e
TP
zone with Eiffellithus
eximius and Zeugrhabdothus diplogrammus (sample
MB001Z1);
2) upper Campanian UC16a–b
BP
zone with Broinsonia
parca constricta and Monomarginatus quaternarius (sample
MB026B5);
3) lower Maastrichtian UC17–18 Reinhardtites levis and
Biscutum magnum (samples MB026B4 and MB001Z3).
The oldest level contains low-latitude taxa Uniplanarius
spp., Ceratolithoides spp. (Fig. 6) and Prediscosphaera
grandis together with high-latitude Prediscosphaera stoveri
and Monomarginatus quaternarius. In the uppermost Cam-
panian low-latitude taxa disappear (species of genus Unipla
narius) or occur scarcely (Ceratolithoides aculeus) while
high-latitude taxa increase in quantity (
Micula staurophora,
Kamptnerius magnificus).
Heavy mineral assemblage
In the heavy-mineral fraction from sandstones opaque
minerals prevail over the translucent. The fine-grained sand-
stone from the MB001 section contained garnet-zircon-rutile
assemblage with minor tourmaline and staurolite, while the
MB026 contained garnet-tourmaline-zircon assemblage with
minor rutile, apatite and staurolite (Table 2). The ZTR matu-
rity index shows medium values between 46 and 53 %. Simi-
lar assemblages were also recorded in the Frýdek Formation
west of the type area.
Geochemical proxies
The typical brown grey pelitic rock from the Frýdek
MB001 section shows rather low total organic carbon (TOC)
of 0.53 % (Table 3), sulphur (TS) of 0.25 % and increased
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inorganic carbon (TIC) that corresponds to marl (CaCO
3
of
34 %). The exposed rocks in the Frýdek type area are partly
weathered and the analytical data may be thus affected.
Remarks
The original type outcrop below the Frýdek castle was
very probably destroyed during the construction of a railway
finished in 1871. The slope directly below the castle seems
to be artificially reshaped because of landslide risk and no
outcrops can be seen there. The location of Hanzlíková’s
test trenches is unknown and no map or coordinates were
given (Hanzlíková 1969 and Hanzlíková et al. 1982).
Reworked microfossils and the disturbed stratigraphic or-
der of strata make the type area inappropriate for biostrati-
graphical study and the local zones of Hanzlíková (1969) can
hardly be accepted. Hanzlíková et al. (1982) admitted a dis-
Fig. 6. Marker nannofossils from the Subsilesian Unit. 1 — Broinsonia parca constricta, Frýdek MB026B5; 2 — Eiffellithus eximius, Frý -
dek MB001Z1;
3 — Biscutum magnum, Frýdek MB026B4; 4 — Reinhardtites levis, Frýdek MB026B4; 5 — Monomarginatus quaternarius,
Frýdek MB026B5; 6 — Micula staurophora, Frýdek MB026B4; 7 — Uniplanarius sissinghii, Frýdek MB001Z1; 8 — Uniplanarius tri fi
dus, Frýdek MB0001Z1; 9 — Ceratolithoides aculeus, Frýdek MB001Z1; 10 — Prediscosphaera grandis, Frýdek MB001Z1; 11 — Pre
discosphaera stoveri, Frýdek MB026B4; 12 — Dictyococcites bisectus, Frýdlant MB009; 13 — Reticulofenestra umbilicus, Frýdlant
MB007; 14 — Reticulofenestra minuta, Paršovice MB041D; 15, 16 — Reticulofenestra ornata, Rakov MB036A; 17 — Reticulofenestra
lockeri, Dolní Těšice MB032; 18 — Coccolithus formosus, Frýdlant MB008; 19 — Helicosphaera bramlettei, Frýdlant MB009;
20, 21 — Helicosphaera intermedia, Frýdlant MB008; 22 — Chiasmolithus solitus, Frýdlant MB009; 23 — Chiasmolithus altus, Paršovice
MB041D; 24 — Sphenolithus spiniger, Frýdlant MB009; 25 — Neococcolithus dubius, Frýdlant MB009; 26 — Pontosphaera obliquipons,
MB041D; 27 — Pontosphaera sigmoidalis, Frýdlant MB009; 28 — Pontosphaera latoculata–magna, Rakov MB036A;
29 — Pontosphaera latelliptica, Rakov MB036A; 30 — Pontosphaera pax, Dolní Těšice MB032. 1–14, 16–21, 24, 26–30 — cross-polarized
light, 15, 22, 23 and 25 — plane-polarized light.
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turbance by faults (tectonic slices). Newly observed gravity
folds apparently caused the overturned position of some in-
tervals of the section (Fig. S2 in the Supplementary Material
file and Fig. 4). Some marls contained reworked shallow-
water fauna of bryozoans, cidarids and serpulids (sample
MB026A). A single specimen of Maastrichtian
Abathomphalus intermedius was found together with a late
Campanian nannofossil assemblage in the sample MB001Z2.
The sample MB026B5 contained late Campanian nannofos-
sils and sample MB026B4 early Maastrichtian although they
came from two limbs of a single fold. All these observations
may mean that the strata at the type area are to a smaller or
larger extent part of a slump body.
Frýdlant Formation
History of studies
Eliáš (1993) defined the Frýdlant Formation as a replace-
ment for the terminologically inappropriate name “Submeni-
litic Formation” sensu Menčík et al. (1983).
He did not designate explicitly the type section but
just mentioned “environs of Frýdlant nad
Ostravicí, in particular, Ostravice riverbed”
which should be accepted as the type area.
Müllerová (1961) published the first biostrati-
graphic evaluation of the outcrops in this area
based on foraminifers. She assigned the strata
to the Late Eocene of the Subsilesian Unit. Un-
fortunately, she did not specify the position of
studied samples along the river. Some outcrops
in the Ostravice riverbed were assigned by
mistake to the Menilite Formation on geologi-
cal maps (Roth 1964, Menčík and Tyráček
1985, Menčík 1987). Menčík et al. (1983)
speculated about the presence of the Šitbořice
Member (Menilite Fm.) in Frýdlant referring
to an unpublished report by Eva Hanzlíková on
the biostratigraphy of the Menilite Formation.
Nevertheless, Hanzlíková wrote about clay-
stones underlying the menilite cherts (no longer
exposed).
Description of outcrops
In the Ostravice valley at Frýdlant nad Os-
travicí light grey mottled marlstones and
brown grey mudstones are exposed in a series
of outcrops. Varicoloured clays/claystones in
Sibudov creek and a facies of dark grey clay-
stones south of its tributary are also a part of
the same area (Fig. S3 in the Supplementary
Material file).
MB006. Dark grey brown calcareous mud-
stone with poorly preserved bivalve fauna is
exposed in the high riverbank of the Ostravice.
MB007. Light brown grey marlstone out-
crops along the right riverside (Fig. 7C).
MB008. Low outcrops in the riverbed near
the right bank consist of grey brown calcareous
claystone.
MB009. Extensive outcrops in the riverbed consist of bio-
turbated light brown grey marlstones (Fig. 7A).
MB010. Extensive outcrops in the riverbed and high right
bank consist of the same marlstones as at MB009. The bio-
turbated marlstones (Fig. 7B) are interbedded with dark
brown grey mudstones several metres thick.
MB011. Small, disturbed outcrops of green grey, brown
grey and grey non-calcareous clays are situated in the bed of
Sibudov creek. The clays include a lens-like turbidite layer
up to 4 cm thick of grey calcareous glauconitic sandstone
with ripple marks.
MB012. Green grey, brown grey and grey non-calcareous
clays with hairy laminae of silty sandstone are exposed in
meanders of Sibudov creek.
MB013. Green brown non-calcareous silty claystone ex-
posed in a small right stream cut.
MB014. Brown grey non-calcareous silty clay exposed in
a left stream cut includes 20 cm thick lens-like concretion of
grey non-calcareous pelocarbonate (Fig. 8).
Table 2: Quantitative analysis of the translucent heavy minerals in psammites.
Values express the relative number of grains in %. ZTR — maturity index (see
Methods for details).
Table 3: Total inorganic carbon (TIC), organic carbon (TOC) and sulphur (TS) in
typical lithotypes from the type localities.
locality
Frýdek
Frýdek
Sibudov
Rakov
Ženklava
Ženklava
sample
MB001Z4
MB026
MB011
MB037
MB046
MB050
garnet total
41.42
43.02
0.00
12.22
96.14
92.69
zircon idi.
5.02
4.88
20.00
2.89
0.08
0.14
zircon ov.
21.76
7.54
68.00
41.11
0.08
0.14
apatite
1.26
5.10
1.50
1.11
1.48
2.90
rutile
21.34
8.43
8.50
22.78
1.07
1.79
tourmaline
5.65
25.06
0.00
3.11
0.49
1.93
epidote
0.00
0.00
0.00
0.33
0.08
0.00
staurolite
2.30
3.99
0.00
6.22
0.08
0.00
amphibole
0.00
0.00
0.00
1.11
0.00
0.00
titanite
0.00
0.44
0.50
0.11
0.08
0.00
kyanite
0.00
0.00
0.00
7.33
0.00
0.28
monazite
0.42
0.22
0.00
0.11
0.16
0.00
chromspinel
0.21
0.00
0.50
0.11
0.16
0.00
glaucophane
0.00
0.00
0.00
0.33
0.08
0.00
brookite
0.63
0.44
0.50
0.00
0.00
0.00
sillimanite
0.00
0.00
0.00
0.89
0.00
0.00
anatase
0.00
0.22
0.50
0.00
0.00
0.00
other
0.00
0.66
0.00
0.22
0.00
0.14
grain count
484
451
200
901
1217
729
ZTR (%)
53.1
45.9
96.5
69.8
1.7
4.0
locality
sample
lithology
TIC
TOC
TS
formation
Frýdek
MB001Z3
claystone
4.06
0.53
0.25
Frýdek Fm.
Frýdlant n. O.
MB007
marlstone
6.33
<0.05
0.40
Frýdlant Fm.
MB010
marlstone
5.98
0.18
0.62
MB021
claystone
<0.05
1.39
1.31
Rakov
MB036
chert
3.28
1.34
0.19
Menilite Fm.
Horní Těšice
MB043Š4
chert
<0.05
0.87
0.21
MB043Š6
claystone
<0.05
3.03
0.23
MB044E
marl
4.46
4.35
0.13
Dolní Těšice
MB032A
marlstone
7.89
1.73
<0.05
MB032B
claystone
4.99
1.95
<0.05
Ženklava
MB047A
claystone
<0.05
2.39
1.95
Ženklava Fm.
MB047B
claystone*
0.55
3.2
2.34
MB050
claystone
0.44
1.47
<0.05
MB051
clay
1.10
1.14
0.24
* concretion
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MB021. Small cut along
a right tributary to the Ostravice
river exposed dark grey non-cal-
careous silty claystone intercala-
ted with 2 mm thick siltstones
(Fig. 7D).
MB022. Small outcrop of grey
non-calcareous silty claystone
among the roots of an old tree.
MB023. Small exposure of
mottled (bioturbated) pale brown
marlstone.
MB024. High right riverbank
of the Ostravice with brown grey
and grey brown calcareous mud-
stones with light Chondrites bur-
rows.
Lithology and sedimentology
Generally the Frýdlant Forma-
tion in the type area consists of
three lithofacies:
1) Whitish weathered, light
brown grey mottled marlstones
intercalated with brown grey cal-
careous mudstones — silty clay-
stones (MB006–MB010, MB023,
MB024). Locally intensively bio-
turbated horizons were observed.
Rare slump layers consisting of
brown grey mudstone matrix
with intraclasts of marlstone
occur.
2) Dark grey non-calcareous
silty claystones (MB021).
3) Grey, brown grey and green
grey non-calcareous clays with
hairy-thin laminae of silt-
stone and sandstone (MB011–
MB014).
A thin section of the light grey
marlstone (sample MB010)
shows prevailing matrix com-
posed of clay minerals and car-
bonate. Silty admixture is
composed of subangular to angu-
lar quartz about 0.05 mm in
diameter (dominant), K-feldspar
and plagioclase (minor), and
phyllosilicates: muscovite, bio-
tite, chlorite and glauconite (5–
10 mod. %). Bioclasts (mainly
foraminifer tests) form about
40 mod. % of the clastic compo-
nent.
Sandstones are very rare and
usually form laminae up to
10 mm. The only sandstone sam-
ple useful for microscopic study
Fig. 7. Frýdlant Formation at Frýdlant nad Ostravicí: A — bedded bioturbated marlstones
(MB009); B — Chondrites–Planolites ichnofabric in the marlstone (MB010); C — platy brown
grey calcareous mudstones (MB007); D — dark grey non-calcareous claystones (MB021). Photo-
graphs: M. Bubík, 2012–2014.
Fig. 8. Lithology and sedimentology of the Frýdlant Formation at selected sections in Frýdlant
nad Ostravicí; samples indicated by asterisk.
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was medium-grained calcareous sandstone from Sibudov
Creek (MB011; Fig. 9). The rock is poorly sorted and textural-
ly immature. Basal-type cement is composed of carbonate,
which corrodes clastic grains. Psammitic clasts comprise
about 0.3 mm (exceptionally 0.9 mm) angular quartz grains
(dominant), glauconite (about 5 mod. %), feldspars (up to
5 mod. %), chlorite (2–3 mod. %), micas (up to 2 mod. %),
bioclasts (foraminifers, bryozoans; about 1 mod. %) and
rarely sub-oval to oval lithoclasts of gneisses and basic vol-
canites. Monocrystallic quartz prevails over aggregate
quartz. K-feldspar prevails over plagioclase.
Fossil record and biostratigraphy
The Frýdlant Formation is poor in macrofauna. Unidenti-
fied bivalves found in grey brown silty marlstones are proba-
bly reworked from shallower habitats (MB006). Intensive
but monotonous Chondrites–Thalassinoides ichnofabric in
mottled marlstones indicate a low-diversity burrowing infau-
nal community (MB010). In the intercalations of much-less
bioturbated grey brown mudstones light-coloured Chon
drites intricatus is common (MB010, MB024).
Middle to Late Eocene marlstones contain abundant fora-
minifers. Benthic taxa prevail over planktonics. Calcareous
benthics Homalohedra apiopleura, Siphonodosaria gracil
lima, Biapertorbis alteconicus, Svratkina perlata, Cibici
doides grimsdalei, Cibicides amphisyliensis, Nuttallides
truempyi, Bolivina spp., Angulogerina spp., Globocassidulina
spp., Reussella sp. prevails over agglutinated forms Rhab
dammina spp., Bathysiphon robusta, Dolgenia lata, Reticu
lophragmium gerochi, R. amplectens, Spiroplectammina
navarroana, Karrerulina coniformis etc. Foraminifer micro-
fauna is accompanied by sponge spicules, echinoid spines
and pyritized diatoms “
Coscinodiscus”. Brown grey calca-
reous mudstones also contain frequent prasinophyte cysts
Tasmanites sp.
Non-calcareous dark grey and varicoloured claystones
contain a flysch-type agglutinated foraminifer assemblage
with Saccorhiza sp., Hyperammina nuda, Bathysiphon
gerochi, Nothia sp., Lagenammina sp., Ammosphaeroidina
pseudopauciloculata,
Spiroplectammina
navarroana,
Karrerulina spp. etc. Silicified cores of radiolarians
(Spumellaria) and pyritized planktonic diatoms are
common.
The following stratigraphic levels were recognized based
upon planktonic foraminifers and calcareous nannofossils:
1) lowermost Eocene with solely agglutinated foraminifer
assemblages containing Pseudonodosinella elongata
(Fig. 10.1) , Rzehakina minima (Fig. 10.2) and Plectorecur
voides parvus (dark grey non-calcareous mudstones MB022,
varicoloured non-calcareous clays MB011, MB013 and
MB014);
2) Lutetian–Bartonian transition: calcareous nannofossils
of the NP16 zone with Sphenolithus spiniger, Chiasmolithus
solitus, and rare Reticulofenestra umbilicus — Fig. 6; plank-
tonic foraminifera of the E10–E11 biochron with Acarinina
medizzai, A. bullbrooki and Jenkinsina columbiana — Fig. 10
(MB007, MB009);
3) Bartonian–Priabonian transition: calcareous nannofos-
sils of the NNTe11B zone (lower part of NP18) with Heli
cosphaera bramlettei, Neococcolithus dubius and
Dictyococcites bisectus — Fig. 6; planktonic foraminifers
younger than mid E13 zone with Turborotalia increbescens
— Fig. 10 (MB006).
4) Eocene–Oligocene transition: calcareous nannofossils
of the NP21 zone with Coccolithus formosus, Helicosphaera
cf. intermedia, H. euphratis and Pontosphaera obliquipons
— Fig. 6 (MB008).
Heavy mineral assemblage
The only available sandstone sample for heavy mineral
analysis was medium-grained calcareous sandstone (Sibudov
MB011). The heavy mineral fraction was strongly dominated
by opaque minerals. The zircon-rutile assemblage of translu-
cent heavy minerals has a very high content of zircons, espe-
cially oval shaped (Table 2). The ZTR maturity index is
therefore high (96.5 %) and indicates a chemically mature
source area and mechanical destruction of mesostable and
unstable minerals.
Geochemical proxies
The TOC and TS values (Table 3) in mottled marlstones
from Ostravice riverbed (MB007, MB010) are relative low
and indicate oxic bottom conditions during the deposition.
Dark grey claystone from the Frýdlant MB021 outcrop dif-
fers by elevated TOC and TS and very low carbonate content
that illustrate dysoxic bottom conditions and negligible car-
bonate content.
Remarks
Eliáš (1993) characterized the environs of Frýdlant nad
Ostravicí as an area with „illuminative sections of four fun-
damental facies of the formation“, this means facies of mot-
tled claystones, black grey claystones, variegated claystones
and Stráž-type sandstones (Menčík et al. 1983), but does not
mention the fifth facies of submarine slumps (Eliáš 1998). In
fact just two of these facies were confirmed during detailed
field observations in the type area: mottled claystones and
black grey claystones. The first mentioned facies comprises
Fig. 9. Thin section of calcareous sandstone with glauconite and
foraminifer Lenticulina, XPL, sample Sibudov MB011.
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light-weathering marlstones (MB009, MB010). These marl-
stones at first sight recall the Dynów Marlstones of the Meni-
lite Formation which confused various authors of geological
maps (Menčík et al. 1983, Menčík & Tyráček 1985, Menčík
1987). Brown grey mudstones were also used in the past as
a diagnostic rock type for the Menilite Formation. From this
point of view the type area is inappropriate. The environs of
Třinec, where all five mentioned facies are exposed in nu-
merous natural outcrops, would be a better choice for the
type area. Revision of the Frýdlant Formation should be con-
sidered.
Menilite Formation
History of studies
The Menilite Formation is an important lithostratigraphic
marker in Carpathian lithostratigraphy. It was first described
in Moravia and its type section/area should be accepted only
here. Glocker (1844) introduced the Menilite Formation
based on outcrops in the area roughly between Kelč and
Bystřice pod Hostýnem. His initial find of the diagnostic
rock type — laminated menilite chert — was situated in the
small village of Mrlínek about 2 km north of Bystřice pod
Hostýnem. Subsequently he found menilite cherts and other
associated rock types further to the west near Sovadina, near
Lhotsko and at Horní Těšice, Dolní Těšice, Rakov and Paršo-
vice near Kelč. Glocker did not designate the type section be-
cause in his times the concept of the type section still did not
exist. Incidentally, the area of Glocker’s field observations
covers outcrops of the Menilite Formation in three different
tectonic units: Ždánice, Subsilesian and Silesian nappes.
This was a very happy choice, because the type area allows
comparison of common features and differences between
facies of the Menilite Formation in various tectonic units.
In the 170 years since Glocker’s times, no attempt has been
undertaken to find and describe the original historical locali-
ties in detail. Jurášová (1974) described calcareous nanno-
fossils as well as reporting the planktonic-foraminifer
assemblage of the Subchert Member from Horní Těšice.
Nothing more was published about the stratigraphy or
palaeontology of these localities.
Description of outcrops
Among the historical localities of Glocker (1844) Horní
and Dolní Těšice belong to the Subsilesian Unit. Rakov, Par-
šovice, Lhotsko and Sovadina belong to the Ždánice Unit.
No outcrop of the Menilite Formation and even no rock
debris were newly observed in ploughed fields near Lhotsko.
The small quarry in Mrlínek, where Glocker (1844)
Fig. 10. Selected marker foraminifers from the Maastrichtian to lowermost Miocene of the Subsilesian Unit. 1 — Pseudonodosinella elon
gata, Frýdlant MB022; 2 — Rzehakina minima, Frýdlant MB022; 3, 4 — Reticulophragmium gerochi, Frýdlant MB008; 5–8 — Rugoglo
bigerina rugosa, Frýdek MB001Z3; 9–12 — Turborotalia increbescens, Frýdlant MB006; 13 — Jenkinsina columbiana, Frýdlant
MB009A; 14 — Pseudohastigerina naguewichiensis, Paršovice MB041F; 15, 16 — Acarinina medizzai, Frýdlant MB009B; 17 — Acarin
ina cf. medizzai, Paršovice MB041F; 18 — Turborotalita quinqueloba, Ženklava MB051; 19–20 — Cassigerinella chipolensis, Ženklava
MB051. 1–5, 8, 10–12 — optical microscope; 6–7, 9, 13–20 — SEM microscope. Scale bars: 1–12 — 100 µm, 13–20 — 40 µm.
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discovered menilite cherts, does not exist any more and its
location is forgotten. Newly observed outcrops at Mrlínek
will be described in another paper dealing with type sections
of the Silesian Unit.
Dolní and Horní Těšice area (Fig. S4 in the Supplementary
Material file):
MB032 Dolní Těšice. In an entry of a badger burrow on
a side of a small hill, pale brown laminated marlstone with
a 3 cm intercalation of brown marl was observed. The marl-
stone debris on the slope contains the remains of sharks and
fish including articulated fish skeletons. (Dynów Mb.)
MB033 Dolní Těšice. Debris of the pale brown marl-
stone and menilite chert covers the surface of the ploughed
field. Isolated fish and shark remains are common. (Dynów
Mb.)
MB043 Horní Těšice. Light brown silicified claystones
with few menilite chert intercalations were newly excavated
beneath loam in a series of 6 test pits along an old road over
a distance of 18 m. (Chert Mb.)
MB044 Horní Těšice. The right cut of a small stream ex-
posed slices and buddines of clays and marls of various levels
of the Eocene within a strongly tectonically disturbed zone.
A block of grey brown silty marl/marlstone to siltstone of the
Subchert Member was found in this zone (Fig. 11).
MB046 Horní Těšice. Pale brown marlstone crops out in
the steep landslide scarp. (Dynów Mb.)
Rakov area (Fig. S5 in the Supplementary Material file):
MB034 Rakov. Debris of brown grey laminated menilite
cherts on the ploughed field. (Chert Mb.)
MB035 Rakov. Eluvial clay with debris of grey non-cal-
careous siltstones and few brown grey menilite cherts on the
ploughed field (Chert Mb.+Němčice Fm.?).
MB036 Rakov. Small abandoned quarry opened on
a small hill exposes pale grey brown marlstone intercalated
with dark brown grey non-calcareous mudstone and banks of
brown laminated menilite chert (Fig. 11). (Dynów Mb.)
MB037 Rakov. Debris of grey brown laminated and brec-
ciated menilite cherts on a ploughed field. The cherts con-
tained rare lenses of fine-grained glauconitic sandstone.
(Chert Mb.)
MB038 Rakov. Small outcrop of menilite chert on the
margin of a ploughed field. (Chert Mb.)
MB039 Rakov. Abandoned quarry(?) exposes pale brown
grey siliceous “shale”. (Chert Mb.)
MB040 Rakov. Debris of siliceous “shale”, menilite
cherts and Dynów-type marlstone (in proportion 10:7:3) on
the ploughed field. (Chert Mb.+Dynów Mb.)
Paršovice area (Fig. S6 in the Supplementary Material
file):
MB041 Paršovice. Cut around house foundations exposed
green calcareous and non-calcareous clays and light brown
grey sandy marl (Němčice Fm. with Sheshory Mb.) and
overlying laminated light grey brown marl intercalated with
dark brown clay (Subchert Mb.).
G041 Paršovice. Dark brown menilite chert on ploughed
field. (Chert Mb.)
G042 Paršovice. Menilite cherts on ploughed field.
(Chert Mb.)
O099 Paršovice. Pale beige marlstone in a road cut near
a cemetery. (Dynów Mb.)
Sovadina area (Fig. S7 in the Supplementary Material
file):
MB001 Sovadina. Abundant debris of various types of
brown and grey menilite cherts covers a ploughed field.
(Chert Mb.)
MB002 Sovadina. Debris of light grey brown marl and
claystone were found in a pile dug from a water well.
(Dynów Mb.)
Lithology and sedimentology
Generally, the Menilite Formation consists mainly of
pelitic, carbonate and siliceous sedimentary rocks of pelagic
origin and rich in organic matter (Fig. 12). The Formation
can be divided into four formal members in all tectonic units
based on characteristic rock types (Stráník 1981). The basal
Subchert Member is characterized by brown marls. The
overlying Chert Member contains “menilite cherts”, which
may be more precisely classified as opal silicites. The over-
lying Dynów Member consists mainly of Dynów-type marl-
stone, which can also be classified as nannofossil clayey
limestone. A thin section of the marlstone (sample MB032)
shows sporadic phosphatic fish remains and very rare sub-
angular quartz in highly prevailing fine matrix. Intercalated
thin laminae of graded siltstone contain 0.005–0.01 mm
sub-angular to angular quartz grains and rarely small chips of
muscovite and aggregates of glauconite. The Šitbořice Mem-
ber in the upper part of the Formation consists mainly of
brown and light grey claystones.
Small lithological differences between different units re-
flect different original positions within the Silesian Basin.
The Subchert Member in the Subsilesian Unit consists of
dark grey-brown silty marls and siltstones, while in the
Ždánice Unit we find pale grey brown laminated marls inter-
calated with dark brown claystones. The Chert Member in
the Subsilesian Unit consists predominantly of claystones
intercalated with laminated menilite cherts, while in the
Ždánice Unit menilite cherts dominate over silicified clay-
stones. The Dynów-type marlstone is nearly identical in both
units. In the Ždánice Unit it includes up to 55 cm thick lay-
ers of laminated menilite chert and thin intercalations of silty
claystone. Exact comparison is, anyway, limited by fragmen-
tary sections. At present time the Šitbořice Member is not
exposed in the type area. Slightly calcareous grey, brown and
dark grey clays of this member were encountered in a shal-
low borehole between Býškovice and Opatovice nearby.
While the Subchert and Šitbořice members comprise
hemipelagites, the menilite cherts were deposited originally
as diatom oozes and the Dynów-type marlstones as coccolith
oozes. Turbidites are a subordinate component of all four
members and usually form several mm thick graded laminae
of siltstone or very fine sandstone, less frequently with rip-
ples. Gravity folds of mm to m scale were frequently ob-
served in the laminated menilite cherts and marls of the
Dynów Member (Fig. 11B).
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Fossil record and biostratigraphy
Abundant fish remains are a characteristic feature of the
Menilite Formation. The Chert Member in Horní Těšice
(MB043) contained fish scales identified as (?)Sardinella
sardinites, Palimphyes? sp. and an unidentified representa-
tive of Myctophidae. In the Dynów Member near Dolní
Těšice (MB032 and MB033) the
following isolated fish remains
were found: (?) Sardinella sar
dinites (Heckel), Gadidae indet.,
Zaenopsis? sp., Oligophus
moravicus (Pauca), articulated
specimens of Scopeloides glaris
sianus (Agassiz) and gill rakers
of shark
Keasius parvus Leriche.
Fish otoliths were recovered
from the Subchert member at
Paršovice (MB041).
The Sheshory Marl directly
underlying the Menilite Forma-
tion at Paršovice (sample
MB041D) contained the plank-
tonic foraminifera Chiloguem
belina ototara, Pseudohastigerina
naguewichiensis, Tenuitella spp.,
Subbotina eocaena, S. angiporoi
des, S. utilisindex, Globigerina
officinalis, Dentoglobigerina ga
lavisi, D. tripartita, Globotur
borotalita ouachitaensis etc. and
benthic foraminifera Dolgenia
lata, “Rhizammina” sp., Bolivina
spp., Lobatula lobatula, Svratkina
perlata, Gyroidinoides, Melonis,
Cibicidoides, Biapertorbis, Val
vulineria, Oridorsalis etc. The
abundant and diversified cal-
careous-nannofossil assemblage
(30 taxa) is dominated by the ge-
nus Reticulofenestra (mainly
R. minuta) and contains repre-
sentatives of Helicosphaera,
Pontosphaera, Zygrhablithus and
Lanternithus indicative for shal-
lower habitats. The assemblage
can be assigned to the upper part
of the NP22 zone (Kiscellian)
with Reticulofenestra umbilicus
and Chiasmolithus altus.
The Menilite Formation has
characteristic assemblages of
foraminifers and calcareous nan-
nofossils specific for each mem-
ber of the formation. The
assemblages are more or less of
low diversity. The Subchert
Member at Paršovice (samples
MB041E and F) contained
a planktonic foraminifer assem-
blage with Globigerina officinalis, G. praebulloides,
Pseudohastigerina naguewichiensis, Tenuitella gemma and
Chiloguembelina ototara of the Eocene-Oligocene transition
(biochron E16–O1). Benthic foraminifer assemblage com-
prises representatives of Cibicidoides, Bolivina and Angulo
gerina prevailing over Globocassidulina subglobosa,
Fig. 11. Menilite Formation in the type area: A — grey brown platy claystone of the Subchert
Member (Horní Těšice MB044); B — Dynów Marlstones interbedded with menilite cherts with
synsedimentary fold (Rakov MB036). Photograph: M. Bubík, 2014.
Fig. 12. Lithology and sedimentology of the Menilite Formation in the type area; samples indicated
by asterisk.
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Biapertorbis biaperturatus, Reussella sp. and the last ele-
ments of flysch-type agglutinated fauna: Hyperammina? sp.,
Ammodiscus sp., Paratrochamminoides sp. in less calcareous
horizons (sample F). Compared with the underlying Sheshory
Marl, the calcareous nannofossil assemblage with 19 taxa
contains more Coccolithus spp. but less shallow-water ele-
ments like Pontosphaera spp., Helicosphaera spp. and
Chiasmolithus altus (MB041F). It can be assigned to the up-
per part of the NP22 zone with Reticulofenestra umbilicus.
The laminated marl has abundant pteropods Spiratella? sp.
on bedding planes (sample E). Marlstone of the Subchert
Member from Horní Těšice (MB044E) contained poor
planktonic foraminifer fauna with Globigerina officinalis
and Tenuitella brevispira. The benthic assemblage comprises
Bolivina vaceki, Globocassidulina subglobosa, Cibicidoides
sp. and Biapertorbis sp. Calcareous nannofossils from Horní
Těšice were described by Jurášová (1974).
The soft claystones of the Chert Member from Horní
Těšice (MB043Š5) contained just scarce and fragmentary
sponge spicules. Foraminifers are primarily missing and
a single find of a pyrite cast of an unidentified benthic fora-
minifer may be redeposited.
Relatively abundant microfauna was recovered from pale
brown marls of the Dynów Member from Sovadina
(MB002A) and Rakov (MB036A). It comprises fish bones,
sponge spicules, foraminifers and ostracods. The ostracods
are smooth-shelled forms recalling fresh/brackish-water
taxa. Together with fish remains they may be autochthonous
while the foraminifer fauna is very probably completely re-
worked. The plankton comprise Palaeogene Globigerina
praebulloides, G. officinalis, Dipsidripella danvillensis, and
Cretaceous Macroglobigerinelloides bollii, Muricohedber
gella delrioensis, M. planispira and Heterohelix planata.
Benthic foraminifera comprise long-ranging taxa: “Rhizam
mina” sp., Kalamopsis? sp., Ammodiscus cf. cretaceus,
Globocassidulina subglobosa, Bolivina vaceki, Cibicides
amphisyliensis, Trifarina sp., Osangularia sp., Cibicidoides
spp., Escornebovina sp., Gavelinella sp. etc. Low-diversity
calcareous nannoplankton comprises Reticulofenestra lockeri,
R. cf. ornata and Pontosphaera pax (Dolní Těšice MB032)
or, more typically, bloom of Reticulofenestra ornata accom-
panied by scarce Pontosphaera pax, P. latelliptica and
P. magna (Rakov MB036A). Reworked nannofossils from
older Palaeogene and Upper Cretaceous strata were also re-
corded. Reticulofenestra ornata may have adapted to hyposa-
line waters and Pontosphaera pax to lagoonal habitats
(Aubry 1990). Blooms of Reticulofenestra ornata were re-
corded within the NP23–NP24 zone interval of the Western
Carpathians (Švábenická et al. 2007).
Heavy mineral assemblage
Psammitic rocks in the type area of the Menilite Formation
are practically missing. Rare thin lenses of fine-grained glau-
conitic sandstone from laminated menilite cherts from Rakov
(MB037) were used for the heavy mineral analysis. The
quantity of opaque and translucent heavy minerals is nearly
equal. The assemblage of translucent heavy minerals was
surprisingly rich and may be classified as zircon-rutile-gar-
net, with relatively important admixture of metamorphoge-
nous minerals: kyanite, staurolite and tourmaline. Accessoric
presence of glaucophane indicates a high-pressure metamor-
phic source. Good preservation of mesostable and even un-
stable minerals may be explained by the sealing ability of
cherts against dissolution and leaching. The ZTR maturity
index is relatively high and strongly contrasts with very low
values in the overlying Ženklava Formation.
Geochemical proxies
A marlstone of the Subchert member has the highest TOC
among the analysed set from the Subsilesian Unit (4.35 %,
Table 3) indicating the anoxic conditions during the deposi-
tion. The siliceous claystone of the chert member showed
TOC of 3 %. The menilite chert from the Chert Member and
Dynow Member showed lower TOC which may be affected
by partial oxidation of the organic matter. Marlstone and
marl from the Dynów Member (Dolní Těšice MB032) have
TOC as high as 1.7–2 % which indicates the anoxic condi-
tions confirmed by taphonomic features (articulated fish
skeletons). Another interesting finding suggests that some
menilite cherts included in the Dynów Member possess TIC
indicating a carbonate content of about 27 % and may be
classified rather as siliceous marlstones (Rakov MB036).
Remarks
The outcrops of the Menilite Formation at original locali-
ties of Glocker (1844) represent just small fragments of its
total thickness that may be estimated at about 50 m. None of
the newly studied outcrops exceeds the thickness of two me-
tres and can hardly be proposed as the type section of the for-
mation. None of the studied outcrops exposes the boundary
between any of the four members of the formation. For now
it seems to be reasonable just to accept the type area between
Paršovice and Bystřice pod Hostýnem.
Ženklava Formation
History of studies
The Ženklava Formation was introduced by Eliáš (1998).
In the English summary of the monograph he specified the
type locality as a creek 150 m southwest of a chapel in Žen-
klava. In the type description of the formation Eliáš (l.c.) did
not provide any petrographical, sedimentological or micro-
palaeontological data pointing to badly weathered rocks. In
previously published geological maps the Ženklava Forma-
tion in Ženklava is assigned partly to the Frýdlant Fm., part-
ly to the Menilite Fm. (Menčík & Tyráček 1985; Roth 1989).
Description of outcrops
The type locality is situated on the western border of the
Ženklava Tectonic Window. Besides the place designated by
Eliáš (1998), isolated outcrops of the Formation continue up-
stream along the creek (Fig. S8 in the Supplementary Material
file).
MB046 Ženklava. Brown grey non-calcareous silty clay-
stones with subordinate laminated siltstones and fine-grained
calcareous sandstones in a few banks up to 20 cm thick are
exposed in several small isolated outcrops in the creek.
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Fig. 14. Type locality of the Ženklava Formation at small creek in
Ženklava. Tower of the Ženklava chapel visible at the mid top of
picture. Photograph: M. Bubík, 2014.
Fig. 13. Lithology and sedimentology of the Ženklava Formation at selected isolated outcrops at
the type area; samples indicated by asterisk (MIC — micropaleontology, GCH — geochemistry).
Fine-grained calcareous sand-
stones are subordinate in banks
up to 20 cm thick. In thin section
the calcareous sandstone (sample
MB046) reveals poorly sorted
structure. Carbonate cement can
be classified as pore-type or basal
in places and corrodes some clas-
tic grains. Sub-angular to sub-
oval sand grains range in size
between 0.2–0.3 mm. The quartz
grains (both monocrystallic and
aggregate) dominate over K-feld-
spar and plagioclase (10–15
mod. %), muscovite, biotite,
chloritized biotite, chlorite and
rarely glauconite. Plagioclase prevails over K-feldspar. Pse-
fitic admixture comprises pebbles of gneisses, mica schists
and volcanites (volcanic glass?).
Claystones, siltstones and sandstones of the Ženklava For-
mation are mostly muddy turbidites deposited in bathyal.
The sandstones possess usually planar lamination (Tb) and
some siltstones showed ripples (Tc–d). Gravity fold ob-
served at MB050 is evidence of rapid deposition and slope
failure (Fig. 26). Micropalaeontological analysis of rocks
from MB048 proved presence of mudflow containing micro-
fossils from older formations of the Subsilesian Unit and
exotic block of Upper Jurassic limestone.
Fossil record and biostratigraphy
The prevailing silty non-calcareous claystones contain
a pseudoassociation of calcareous and agglutinated foramini-
fers, sponge spicules and fish bones with abundant reworked
component. The reworked species Praemurica inconstans,
Subbotina triloculinoides, Muricohedbergella planispira,
Macroglobigerinelloides bollii, Haplophragmoides decussa
tus, Paratrochamminoides olszewskii and Cibicidoides spp.
came from various levels of the Upper Cretaceous to Eocene
(sample MB046A). More reworked fauna was recovered
from clayey matrix of mudflow (sample MB048A). The
planktonic foraminifera Rotalipora appenninica, Whiteinella
baltica, Pseudotextularia elegans, Globotruncanella peta
loidea, Globotruncana arca, Muricohedbergella mon
mouthensis, Globanomalina compressa, Catapsydrax
unicavus and benthic Rzehakina lata–fissistomata trans.,
Spiroplectammina navarroana, S. dentata, Dorothia bulletta,
Ramulina sp., Bolivinoides draco, Nonion troostae, Eouvige
rina gr. elongata come from various levels of the Albian–
Eocene interval and most of them are common taxa of the
Frýdek and Frýdlant formations. A block of exotic limestone
contained the foraminifers Trocholina nodulosa, Paalzowella
feifeli, Spirillina concava, S. kuebleri, holothurian sclerites,
Tasmanites cysts and may be assigned to the Upper Juras-
sic.
The highest proportion of autochthonous foraminifer fau-
na was recorded in the eastern part of the creek — at points
MB049, MB050 and MB051. Sample MB051 contained
planktonic foraminifera Cassigerinella chipolensis, Tenuitella
brevispira, Tenuitellinata angustiumbilicata, and Turboro
MB047 Ženklava. Black grey platy non-calcareous clay-
stones crop out in the left cut of the stream.
MB048 Ženklava. Dark grey calcareous clays with frag-
ments of clayey limestone bank (block?) crop out in the left
bank of the creek (Fig. 13).
MB049 Ženklava. Brown grey silty calcareous claystone
is exposed in the right bank of the creek (Fig. 13).
MB050 Ženklava. Dark grey non-calcareous silty clay to
clayey siltstone in the left bank of the creek contains gravity
fold consisting of grey fine-grained calcareous sandstone
(Fig. 13).
MB051 Ženklava. Weathered soft grey slightly calcare-
ous clay with silty layers crops out in the creek bed (Fig. 14).
This outcrop corresponds to the type section according to
Eliáš (1998).
Lithology and sedimentology: Brown grey silty non-cal-
careous claystones and siltstones are the dominant lithology.
Locally platy black grey non-calcareous claystones stained
on surfaces by limonite may recall claystones of the Menilite
Formation. Calcareous claystones and clays occur along the
eastern part of the creek (MB048, MB049, and MB051).
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talita quinqueloba indicating the late Egerian (Eggenburg-
ian?), accompanied by reworked Heterohelix planata,
Mur
i
cohedbergella planispira, Pseudohastigerina micra,
Acarinina bullbrooki, A. medizzai and A. pseudotopilensis.
The benthic component consists of Glomospira charoides,
“Rhizammina” sp., Spiroplectammina navarroana, Globo
cassidulina subglobosa, Bolivina dilatata, Angulogerina sp.,
Biapertorbis biaperturatus, Escornebovina cf. binominata,
Epistominella sp., Valvulineria sp., Cibicidoides lopjanicus,
Cibicides amphisyliensis etc. The taphocoenosis also con-
tained frequent pyritized planktonic diatoms “Coscinodis
cus” sp. Calcareous nannofossils from the same sample are
completely reworked from the Maastrichtian, Palaeocene, Upper
Eocene and Lower Oligocene. The following species were
identified: Coccolithus eopelagicus, C. pelagicus, Cyclicar
golithus sp., Dictyococcites bisectus, Discoaster cf. multira
diatus, Ellipsolithus distichus, Coccolithus formosus,
R. lockeri, R. minuta, R. ornata, R. umbilicus, Micula stauro
phora, M. murus and Watznaueria barnesiae.
Heavy mineral assemblage
Two samples of fine-grained calcareous sandstone from
Ženklava were analysed for heavy minerals (MB046 and
MB050). The ratio of opaque to translucent heavy minerals
varies. The assemblage of translucent heavy minerals is
clearly garnet type, with high dominance of the index mineral
(96 and 92 %). Very low ZTR maturity indicates enhanced
erosion of fresh metamorphic rocks in the source area.
Generally garnet rich assemblages are typical for proximal
flysch turbidites.
Geochemical proxies
The elevated TOC values in the partly weathered pelitic
rocks of the Ženklava Formation indicate hypoxic conditions
and in the case of black grey platy claystone (MB047A) even
anoxic conditions, which is supported by high sulphur con -
tent and presence of abundant isolated fish bones. According
to the TIC values the CaCO
3
content ranges from 0 % to
9 %. The upper value allows us to classify the rock as cal-
careous clay (MB051).
Remarks
Abundance of reworked microfossils and garnet associa-
tion of the translucent heavy minerals is a characteristic fea-
ture of the Ženklava Formation at the type locality. At the
same time it is typical for the Krosno Formation that is
an analogue of the Ženklava Fm. in each mean. Small and
fragmentary outcrops in Ženklava sufficiently illustrate the
lithological variability of the formation only as a whole. It is
therefore reasonable to extend the type section to the whole
500 m long section of the creek where Egerian strata are
exposed.
Conclusions
In the Subsilesian Unit two original type sections (Frýdek
and Ženklava) and two type areas (Frýdlant nad Ostravicí
and Kelč area) were studied. These localities form the basis
for definition of the four formal formations (Upper Creta-
ceous–lowermost Miocene) that form the sedimentary suc-
cession of the Subsilesian Unit.
A section near the destroyed historical locality below the
Frýdek castle/chateau is newly proposed as a type locality of
the Frýdek Formation.
The particular type section of the Frýdlant Formation was
not specified by the original author. Due to fragmentary out-
crops the type area is newly specified in an area where facies
of dark-grey claystones and mottled marlstones were newly
recorded. Three other fundamental lithofacies of the forma-
tion: variegated beds, Stráž-type sandstones and pebbly
mudstones were not observed at Frýdlant. The hypotype lo-
calities for these three facies should be selected and studied.
As the original type area of the Menilite Formation be-
tween Paršovice and Bystřice pod Hostýnem has only small
isolated outcrops not exceeding 2 m in thickness, the particu-
lar type section for the formation cannot be proposed at the
present moment.
Based on the field observations and study of the Ženklava
Formation at Ženklava, the extension of the type locality to
the whole 500 m long creek section is proposed.
None of the discussed type localities or sections in the
type areas are protected by law, and the stratotype status of the
outcrops is not subject to protection at the present time. The
protection is urgently needed and should be managed soon
for the sake of Carpathian stratigraphy and preservation of
the geological heritage for the future.
Acknowledgements: The study was supported by internal
grant CGS No 321170. We are grateful to Růžena Gregorová
and Tomáš Přikryl for determination of fish remains from the
Menilite Formation. Katarína Holcová kindly assisted with
SEM micrographs.
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Planktonic Foraminifera
Abathomphalus mayaroensis (Bolli, 1951) ex Globotruncana
Abathomphalus intermedius (Bolli, 1951) ex Globotruncana
Acarinina bullbrooki (Bolli, 1957) ex Globorotalia
Acarinina medizzai (Toumarkine et Bolli, 1975) ex Globigerina
Acarinina pseudotopilensis Subbotina, 1953
Cassigerinella chipolensis (Cushman et Ponton, 1932) ex Cassi
dulina
Catapsydrax unicavus Bolli, Loeblich et Tappan, 1957
Chiloguembelina ototara (Finlay, 1940) ex Guembelina
Dentoglobigerina galavisi (Bermúdez, 1961) ex Globigerina
Dentoglobigerina tripartita (Koch, 1926) ex Globigerina
Dipsidripella danvillensis (Howe et Wallace, 1932) ex Globorotalia
Globanomalina compressa (Plummer, 1926) ex Globigerina
Globigerina officinalis Subbotina, 1953
Globigerina praebulloides Blow, 1959
Globotruncana arca (Cushman, 1926) ex Pulvinulina
Globotruncanella petaloidea (Gandolfi, 1955) ex Globotruncana
(Rugoglobigerina)
Globoturborotalita ouachitaensis (Howe et Wallace, 1932) ex Glo
bigerina
Heterohelix planata (Cushman, 1938) ex Guembelina
Jenkinsina columbiana (Howe, 1939) ex Guembelitria
Macroglobigerinelloides bollii (Pessagno, 1967) ex Globigerinel
loides
Muricohedbergella delrioensis (Carsey, 1926) ex Globigerina
Muricohedbergella monmouthensis (Olsson, 1960) ex Globorotalia
Muricohedbergella planispira (Tappan, 1940) ex Globigerina
Praemurica inconstans (Subbotina, 1953) ex Globigerina
Pseudohastigerina micra (Cole, 1927) ex Nonion
Pseudohastigerina naguewichiensis (Myatliuk, 1950) ex Globige
rinella
Pseudotextularia elegans (Rzehak, 1891) ex Cuneolina
Rotalipora appenninica (Renz, 1936) ex Globotruncana
Rugoglobigerina rugosa (Plummer, 1926) ex Globigerina
Subbotina angiporoides (Hornibrook, 1965) ex Globigerina
Subbotina eocaena (Guembel, 1868) ex Globigerina
Subbotina triloculinoides (Plummer, 1926) ex Globigerina
Subbotina utilisindex (Jenkins et Orr, 1973)
Tenuitella brevispira (Subbotina, 1960) ex Globigerina
Tenuitella gemma (Jenkins, 1966) ex Globorotalia
Tenuitella praegemma (Li, 1987) ex Praetenuitella
Tenuitellinata angustiumbilicata (Bolli, 1957) ex Globigerina
Turborotalia increbescens (Bandy, 1949) ex Globigerina
Turborotalita quinqueloba (Natland, 1938) ex Globigerina
Whiteinella baltica Douglas et Rankin, 1969
Benthic Foraminifera
Alabamina dorsoplana (Brotzen, 1940) ex Eponides
Allomorphina obliqua Reuss, 1851
Ammodiscus cretaceus (Reuss, 1845) ex Operculina
Ammosphaeroidina pseudopauciloculata (Mjatliuk, 1966) ex
Cystamminella
Bathysiphon gerochi Mjatliuk, 1966
Bathysiphon robusta (Grzybowski, 1898) ex Dendrophrya
Biapertorbis alteconicus Pokorný, 1956
Biapertorbis biaperturatus Pokorný, 1956
Bolivina dilatata Reuss, 1850
Bolivina vaceki Schubert, 1902
Bolivinoides draco (Marsson, 1878) ex Bolivina
Cibicides amphisyliensis (Andreae, 1884) ex Truncatulina
Cibicidoides grimsdalei (Nuttall, 1930) ex Cibicides
Cibicidoides lopjanicus (Mjatliuk, 1950)
Dolgenia lata (Grzybowski, 1898) ex Ammodiscus
Dorothia bulletta (Carsey, 1926) ex Gaudryina
Eouvigerina elongata (Cole, 1927) ex Uvigerina
Eouvigerina serrata (Chapmann, 1892) ex Textularia
Escornebovina binominata (Subbotina, 1960) ex Eponides
Globocassidulina subglobosa (Brady, 1881) ex Cassidulina
Glomospira charoides (Jones et Parker, 1860) ex Trochammina
Haplophragmoides decussatus Krasheninnikov, 1973
Hemirobulina hamuloides (Brotzen, 1936) ex Marginulina
Homalohedra apiopleura (Loeblich et Tappan, 1953) ex Lagena
Hyperammina nuda Subbotina, 1950
Karrerulina coniformis (Grzybowski, 1898) ex Gaudryina
Lenticulina discrepans (Reuss, 1863) ex Cristellaria (Robulina)
Lobatula lobatula (Walker et Jacob, 1798) ex Nautilus
Nonion troostae Visser, 1951
Nuttallides truempyi (Nuttall, 1930) ex Eponides
Nuttallinella florealis (White, 1928) ex Gyroidina
Paalzowella feifeli (Paalzow, 1932) ex Trocholina
Pararotalia bandyi (Martin, 1964) ex Rotalia
Paratrochamminoides olszewskii (Grzybowski, 1898) ex Trocham
mina
Plectorecurvoides parvus Krasheninnikov, 1973
Praebulimina petroleana (Cushman et Hedberg, 1941) ex Bulimina
Praebulimina reussi (Morrow, 1934) ex Bulimina
Praebulimina triangularis (Marie, 1941) ex Buliminella
Pseudonodosinella elongata (Grzybowski, 1898) ex Reophax
Pullenia marssoni Cushman et Todd, 1943
Pyramidina cimbrica (Troelsen, 1945) ex Pseudouvigerina
Remesella varians (Glaessner, 1937) ex Textulariella
Reticulophragmium amplectens (Grzybowski, 1898) ex Cyclammina
Reticulophragmium gerochi Neagu et al., 2011
Rotorbinella supracretacea (Schijfsma, 1946) ex Discorbis
Rzehakina minima Cushman et Renz, 1948
Rzehakina lata Cushman et Jarvis, 1928
Rzehakina fissistomata (Grzybowski, 1901) ex Spiroloculina
Siphonodosaria gracillima (Cushman et Jarvis, 1934) ex Ellipsono
dosaria
Spirillina concava (Terquem, 1870) ex Cornuspira
Spirillina kuebleri Mjatliuk, 1953
Spiroplectammina dentata (Alth, 1850) ex Textularia
Spiroplectammina navarroana Cushman, 1932
Svratkina perlata (Andreae, 1884) ex Pulvinulina
Trocholina nodulosa Seibold et Seibold, 1960
Calcareous nannofossils
Biscutum magnum Wind et Wise in Wise et Wind 1977
Broinsonia parca constricta Hattner et al. 1980
Cassigerinella chipolensis (Cushman et Ponton, 1932) ex Cassi
dulina
Ceratolithoides aculeus (Stradner 1961) Prins et Sissingh in
Sissingh 1977
Chiasmolithus altus Bukry et Percival , 1971
Chiasmolithus solitus (Bramlette et Sullivan 1961) Locker 1968
Coccolithus eopelagicus (Bramlette et Riedel, 1954) Bramlette et
Sullivan, 1961
Coccolithus formosus (Kamptner 1963) Wise 1973
Appendix 1.
The full names of species mentioned in the text
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Coccolithus pelagicus (Wallich, 1871) Schiller, 1930
Dictyococcites bisectus (Hay et al. 1966) Bukry et Percival 1971
Discoaster multiradiatus Bramlette et Riedel 1964
Eiffellithus eximus (Stover 1966) Perch-Nielsen 1968
Ellipsolithus distichus (Bramette et Sullivan 1961) Sullivan 1964
Helicosphaera bramlettei Müller 1970
Helicosphaera euphratis Haq 1966
Helicosphaera intermedia Martini 1965
Kamptnerius magnificus Deflandre 1959
Micula murus (Martini 1961) Bukry 1973
Micula staurophora (Gardet 1955) Stradner 1963
Monomarginatus quaternarius Wind et Wise in Wise and Wind 1977
Neococcolithus dubius (Deflandre in Deflandre et Fert 1954)
Black 1967
Pontosphaera latelliptica (Báldi-Beke 1974) Perch-Nielsen 1984
Pontosphaera magna Haq 1971
Pontosphaera obliquipons (Deflandre 1954) Romein 1979
Pontosphaera pax (Stradner et Seifert 1980) Aubry 1986
Pontosphaera sigmoidalis (Locker 1967) Aubry 1986
Prediscospaera grandis Perch-Nielsen 1979
Prediscosphaera stoveri (Perch-Nielsen 1968) Shafik et
Stradner 1971
Reinhardites levis Prins et Sissingh in Sissingh 1977
Reticulofenestra lockeri Müller 1970
Reticulofenestra minuta Roth 1970
Reticulofenestra ornata Müller 1970
Reticulofenestra umbilicus (Levin 1965) Martini et Ritzkowski 1968
Sphenolithus spiniger Bukry 1971
Uniplanarius sissinghii Perch-Nielsen 1986
Uniplanarius trifidus (Stradner in Stradner et Papp 1961) Hattner et
Wise 1980.
Watznaueria barnesiae (Black 1959) Perch-Nielsen 1968
Zeugrhabdothus diplogrammus (Deflandre in Deflandre et Fert
1954) Burnett in Gale et al. 1996
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Supplementary Material File
Situations of outcrops and sample localizations
Fig. S1. Situation of sections MB001 and MB026 at Frýdek with
indicated sampling points.
Fig. S2. Outcrop MB026 at Frýdek below an orchard.
Fig. S3. Outcrops of the Frýdlant Formation at Frýdlant nad
Ostravicí.
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Fig. S4. Situation of outcrops of the Menilite Formation between Horní and Dolní Těšice.
Fig. S5. Situation of outcrops of the Menilite Formation near Rakov.
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Fig. S6. Situation of outcrops of the Menilite Formation near
Paršovice.
Fig. S7. Situation of outcrops of the Menilite Formation near
Sovadina.
Fig. S8. Situation of outcrops of the Ženklava Formation at
Ženklava type area.