GeolCarp_Vol67_No3_239

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

, HELENA GILÍKOVÁ

, JIŘÍ OTAVA

and LILIAN ŠVÁBENICKÁ

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

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

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

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

240

BUBÍK, FRANCŮ, GILÍKOVÁ, OTAVA and ŠVÁBENICKÁ

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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.

241

STRATOTYPES OF U. CRETACEOUS–L. MIOCENE FORMATIONS (W CARPATHIANS)

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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

). 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.

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

242

BUBÍK, FRANCŮ, GILÍKOVÁ, OTAVA and ŠVÁBENICKÁ

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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.

243

STRATOTYPES OF U. CRETACEOUS–L. MIOCENE FORMATIONS (W CARPATHIANS)

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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

zone with Eiffellithus

eximius and Zeugrhabdothus diplogrammus (sample

MB001Z1);

2) upper Campanian UC16a–b

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

245

STRATOTYPES OF U. CRETACEOUS–L. MIOCENE FORMATIONS (W CARPATHIANS)

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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

Sibudov

Rakov

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

0.33

0.08

0.00

staurolite

2.30

3.99

0.00

6.22

0.08

0.00

amphibole

0.00

1.11

0.00

titanite

0.00

0.44

0.50

0.11

0.08

0.00

kyanite

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

0.33

0.08

0.00

brookite

0.63

0.44

0.50

0.00

sillimanite

0.00

0.89

0.00

anatase

0.00

0.22

0.50

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

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

246

BUBÍK, FRANCŮ, GILÍKOVÁ, OTAVA and ŠVÁBENICKÁ

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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.

247

STRATOTYPES OF U. CRETACEOUS–L. MIOCENE FORMATIONS (W CARPATHIANS)

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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.

248

BUBÍK, FRANCŮ, GILÍKOVÁ, OTAVA and ŠVÁBENICKÁ

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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.

249

STRATOTYPES OF U. CRETACEOUS–L. MIOCENE FORMATIONS (W CARPATHIANS)

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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).

250

BUBÍK, FRANCŮ, GILÍKOVÁ, OTAVA and ŠVÁBENICKÁ

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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.

251

STRATOTYPES OF U. CRETACEOUS–L. MIOCENE FORMATIONS (W CARPATHIANS)

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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.

252

BUBÍK, FRANCŮ, GILÍKOVÁ, OTAVA and ŠVÁBENICKÁ

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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).

253

STRATOTYPES OF U. CRETACEOUS–L. MIOCENE FORMATIONS (W CARPATHIANS)

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

talita quinqueloba indicating the late Egerian (Eggenburg-

ian?), accompanied by reworked Heterohelix planata,

Mur

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

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.

References

Aubry M.P. 1990: Handbook of Cenozoic calcareous nannoplank-

ton. Book 4: Heliolithae (helioliths, cribriliths, lopadoliths,

and others). Micropaleontology Press, 1–181.

Burnett J.A. (with contrubutions from Gallagher L.T. & Hampton

M.J.) 1998: Upper Cretaceous. In: Bown P.R. (Ed.): Calca-

reous Nannofossil Biostratigraphy. British Micropalaeontol.

Soc. Publ. Ser., Chapman & Hall, London, 132–199.

Cieszkowski M., Golonka J. & Waśkowska A. 2012: An olistolith

interpretation for the Paleocene Szydłowiec Sandstones in the

stratotype area (Outer Carpathians, Poland). Austrian J. Earth

Sci. 105, 1, 240–247.

Eliáš M. 1993: Sedimentological investigation of the Subsilesian

Unit in the Ostrava region. Zpr. Geol. Výzk. 1991, 40–42. (in

Czech)

Eliáš M. 1998: Sedimentology of the Subsilesian Unit. Práce

Českého geologického ústavu 8, 1–48. (in Czech)

Eliáš M. & Hanzlíková E. 1964: Frýdek Beds — type locality

on Castle hill in Frýdek–Místek. Zpr. Geol. Výzk. 1963, 1,

255–256. (in Czech)

Glocker E.F. 1844: Die Menilitformation in Mähren. In: Langer L. &

Schrötter A. (Eds.): Amtlicher Bericht über die einundzwan-

zigste Versammlung deutscher Naturforscher und Aerzte in

Gratz im September 1843. Andreas Leykam’schen Erben,

254

BUBÍK, FRANCŮ, GILÍKOVÁ, OTAVA and ŠVÁBENICKÁ

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

Gratz, 139–141.

Golonka J. 2011: Evolution of the Outer Carpathian Basins. In: Bąk

M., Kaminski M.A. & Waśkowska A. (Eds.): Integrated micro-

fossil records from the oceans and epicontinental seas. Grzy

bowski Foundation Spec. Publ. 17, 3–14.

Hanzlíková E. 1969: The Foraminifera of the Frýdek Formation

(Senonian). Sbor. Geol. Věd, Paleontol. 11, 7–84.

Hanzlíková E. 1972: Carpathian Upper Cretaceous Foraminiferida

of Moravia (Turonian–Maastrichtian). Rozpravy Ústř. Úst.

Geol. 39, 1–160.

Hanzlíková E., Menčík E. & Pesl V. 1953: Remarks to stratigraphy

and tectonics of the Subsilesian and Silesian nappes on the

Nový Jičín map square. Zpr. Geol. Výzk. 1952, 15–18. (in

Czech)

Hanzlíková E., Krhovský J. & Švábenická L. 1982: Calcareous

nannoplankton from the type locality of the Frýdek Forma-

tion (Lower Maastrichtian). Sbor. Geol. Věd, Paleontol. 25,

127–155.

Hochstetter F. 1852: Notiz über eine Kreideschichte am Fusse

der Karpathen bei Friedek in k. k. Schlesien. Jb. K.–K. Geol.

Reichsanst. 3, 4, 33–35.

Hohenegger L. 1852: Geognostische Skizze der Nordkarpathen von

Schlesien und den nächsten Angränzungen (nach dem gegen

wärtigen Stand puncte meiner Erfahrungen). Jb. K.–K. Geol.

Reichsanst. 3, 135–148.

Hohenegger L. 1861: Die geognostischen Verhältnisse der

Nord-Karpathen in Schlesien und den angrenzenden Theilen

von Mähren und Galizien. Erläuterung zu der geognostischen

Karte der Nordkarpathen. Justus Perthes, Gotha, 1–50.

Jurášová F. 1974: Nannoplankton from the Menilitic Formation

(Lower Oligocene) at Dolní Těšice. Věst. Ústř. Úst. Geol. 49,

91–96.

Książkiewicz M. 1951: Explanations to the Sheet Wadowice.

General geological map of Poland, scale 1:50 000. Państw.

Inst. Geol. Warszawa, 1–283. (in Polish)

Liebus A. & Uhlig V. 1902: Über einige Fossilien aus der kar-

patische Kreide. Beitr. Paläontol. Geol. Österr.–Ungarns u. d.

Orients 14, 1–2, 113–130.

Lirer F. 2000: A new technique for retrieving calcareous micro-

fossils from lithified lime deposits. Micropaleontology 46, 4,

365–369.

Martini E. 1971: Standard Tertiary and Quarternary calcareous nan-

noplankton zonation. In: Farinacci A. (Ed.): Proc. 2nd Plank-

tonic Conf., Roma, 1970, Vol. 2. Tecnoscienza, 739–765.

Menčík E. 1987: Geological map of the ČSR. Sheet 25–22 Frýdek-

Místek. Ústřední ústav geologický, Praha. (in Czech)

Menčík E., Adamová M., Dvořák J., Dudek A., Jetel J., Jurková A.,

Hanzlíková E., Houša V., Peslová H., Rybářová L., Šmíd B.,

Šebesta J., Tyráček J. & Vašíček Z. 1983: Geology of Morav-

skoslezské Beskydy Mts. and Subbeskydian Upland.

Ústřední

ústav geologický, Praha, 1–304. (in Czech)

Menčík E. & Tyráček J. 1985: Beskydy Mts. and Subbeskydian Up-

land. Overview geological maps 1 : 100,000. Ústřední Ústav

Geologický, Praha. (in Czech)

Müllerová J. 1961: Microbiostratigraphy of a shale formation in

Frýdlant nad Ostravicí. Sborník vědeckých Prací Vysoké školy

báňské v Ostravě, 7, 4–5, 533–540. (in Czech)

Olszewska B. 1997: Foraminiferal biostratigraphy of the Polish

Outer Carpathians: a record of basin geohistory. Ann. Soc.

Geol. Polon., 67, 325–337.

Roth Z. 1964: Geological map of the ČSSR, Map of pre-Quaternary

formations 1 : 200,000, M–34–XIX Ostrava — M–34–XIII

Strahovice. Ústřední ústav geologický, Praha. (in Czech)

Roth Z. 1971: Die Strukturfazies der äußeren Karpaten in Mähren

und die Klassifizierung ihrer Hüllendecken nach dem tekto-

nischen Stil. Věst. Ústř. Úst. Geol. 46, 4, 233–236.

Roth Z. 1989: Geological map of the ČSR. Sheet 25–21 Nový Jičín.

Ústřední ústav geologický, Praha. (in Czech)

Roth Z. & Hanzlíková E. 1967: Stratigraphy. In: Buday T. (Ed.):

Regional geology of the ČSSR, Part II: Western Carpathians,

Vol. 2. Ústřední ústav geologický, Praha, 113–200. (in Czech)

Růžička B. & Beneš V. 1949: Preliminary report on Foraminifera of

the Frýdek Beds (Upper Cretaceous). Přírodovědecký sborník

ostravského kraje 10, 3, 253–260. (in Czech)

Ślączka A., Kruglov S., Golonka J., Oszczypko N. & Popadyuk I.

2006: Geology and Hydrocarbon Resources of the Outer Car-

pathians, Poland, Slovakia, and Ukraine: General Geology. In:

Golonka J. & Picha F.J. (Eds.): The Carpathians and their fore-

land: Geology and hydrocarbon resources. AAPG Memoir 84,

221–258.

Straník Z. 1981: Lithofaces and correlations of the Menilite Beds in

the Carpathian Flysch Belt in Moravia. Zemní Plyn Nafta 26,

1, 9–18. (in Czech)

Švábenická L. 2012: Nannofossil record across the Cenomanian–

Coniacian interval in the Bohemian Cretaceous Basin and

Tethyan foreland basins (Outer Western Carpathians), Czech

Republic. Geol. Carpath. 63, 3, 201–217.

Švábenická L., Bubík M. & Stráník Z. 2007: Biostratigraphy and

plaeoenvironmental changes on the transition from Menilite

to Krosno lithofacies (Western Carpathians, Czech Republic).

Geol. Carpath. 58, 3, 237–262.

Varol O. 1998: Palaeogene. In: Bown P.R. (Ed.): Calcareous nan-

nofossil biostratigraphy. British Micropalaeontol. Soc. Publ.

Ser., Chapman & Hall, London, 200–224.

Waśkowska A. 2011: Response of Early Eocene deep-water benthic

foraminifera to volcanic ash falls in the Polish Outer Car -

pathians: Palaeoecological implications. Palaeogeogr. Palaeo

climatol. Palaeoecol. 305, 50–64.

255

STRATOTYPES OF U. CRETACEOUS–L. MIOCENE FORMATIONS (W CARPATHIANS)

GEOLOGICA CARPATHICA

, 2016, 67, 3, 239–256

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

Document Outline