GeolCarp_Vol67_No4_303

www.geologicacarpathica.com

GEOLOGICA CARPATHICA, AUGUST

, , ,

doi: 10.1515/geoca-2016-0020

Stratigraphy, plankton communities, and magnetic proxies

JOZEF

MICHALÍK

, DANIELA

REHÁKOVÁ

, JACEK

GRABOWSKI

, OTÍLIA

LINTNEROVÁ

ANDREA SVOBODOVÁ

5,6

, JÁN

SCHLÖGL

, KATARZ NA SOBIE

and PETR SCHNABL

Earth Science Institute of the Slovak Academy of Sciences, Dúbravská cesta 9, P.O. Box 106, 840 05 Bratislava, Slovakia; geolmich@savba.sk

Comenius University, Faculty of Science, De t. of Geology and Palaeontology, Ilkovi ova 6, 842 15 Bratislava, Slovakia;

rehakova@fns.uniba.sk; schlogl@nic.fns.uniba.sk

Polish Geological Institute – National Research Institute, Rakowiecka 4, 00-975 Warsaw, Poland; jacek.grabowski@pgi.gov.pl;

katarzyna.sobien@pgi.gov.pl

Comenius University, Faculty of Science, Dept. of Economic Geology, Ilkovi ova 6, 842 15 Bratislava, Slovakia; lintnerova@fns.uniba.sk

Charles University in Prague, Faculty of Science, Institute of Geology and Palaeontology, Albertov 6, 128 43 Prague, Czech Republic;

andrea.svobodova@natur.cuni.cz

Czech Academy of Sciences, Institute of Geology, Rozvojová 269, 165 00 Prague 6, Czech Republic; schnabl@gli.cas.cz; asvobodova@gli.cas.cz

(Manuscript received December 9, 2015; accepted in revised form June 7, 2016)

A well preserved Upper Tithonian–Lower Berriasian Strapkova sequence of hemipelagic limestones

improves our understanding of environmental changes occurring at the Jurassic/Cretaceous boundary in the Western
Carpathians. Three dino agellate and four calpionellid zones have been recognized in the section. The onset of the
Alpina Subzone of the standard Calpionella Zone, used as a marker of the Jurassic/Cretaceous boundary is de ned by
morphological change of Calpionella alpina tests. Calpionellids and calci ed radiolarians numerically dominate in
microplankton assemblages. The rst occurrence of Nannoconus wintereri indicates the beginning of the nannofossil
zone NJT 17b Subzone. The FO of Nannoconus steinmannii minor was documented in the lowermost part of the Alpina
Subzone. This co-occurrence of calpionellid and nannoplankton events along the J/K boundary transition is typical of
other Tethyan sections. Correlation of calcareous microplankton, of stable isotopes (C, O), and TOC/CaCO

data distri-

bution was used in the characterization of the J/K boundary interval.

C values (from +1.09 to 1.44 ‰ VPDB) do not

show any temporal trends and thus show a relatively balanced carbon-cycle regime in sea water across the Jurassic/
Cretaceous boundary. The presence of radiolarian laminites, interpreted as contourites, and relatively high levels of
bioturbation in the Berriasian prove oxygenation events of bottom waters. The lower part of the Crassicolaria Zone (up
to the middle part of the Intermedia Subzone) correlates with the M19r magnetozone. The M19n magnetozone includes
not only the upper part of the Crassicollaria Zone and lower part of the Alpina Subzone but also the FO of Nannoconus
wintereri and Nannoconus steinmannii minor. The reverse Brodno magnetosubzone (M19n1r) was identi ed in the
uppermost part of M19n. The top of M18r and M18n magnetozones are located in the upper part of the Alpina Subzone
and in the middle part of the Ferasini Subzone, respectively. The Ferasini/Elliptica subzonal boundary is located in the
lowermost part of the M17r magnetozone. A little bit higher in the M17r magnetozone the FO of Nannoconus steinman-
nii steinmannii was identi ed.

J/K boundary, pelagic limestones, microfauna, nannoplankton, stable C and O isotopes, magnetic

susceptibility, northern Tethys.

Introduction

Collection of sedimentological, geochemical and palaeonto-
logical data from complete stratigraphic sections, which can
be used for correlation among candidate stratotypes of stage
boundaries, is one of major goals of the Berriasian Interna-
tional Commission on Stratigraphy (ICS) program. A net-
work of regional stratotypes can provide a continuous record
of both sedimentation and biotic events across the Jurassic/
Cretaceous boundary, and a precise evaluation of all proxies
necessary for exact discrimination of the boundary position.
In the Western Carpathians, the Brodno section (Michalík et
al. 1990, 2009; Houša et al. 1996, 1999) represents the regional
stratotype of the J/K boundary. However, ammonites are rare
and sediment thickness is somewhat reduced in the Brodno

section, and complementary J/K boundary sections were thus
recently studied in the Western Carpathian (Fig. 1):

the Strá ovce section (Borza 1984; Michalík et al. 1990);
the Hlbo a section (Grabowski et al. 2010) and Po rednie
sections in the Tatra Mts. (Grabowski Pszcz kowski
2006; Grabowski et al. 2013).

Remarkable advances in calpionellid and nannoplankton

biostratigraphy across the J/K boundary interval have been
published on the basis of Tethyan Jurassic/Cretaceous boun-
dary (JKB) sections (Lukeneder et al. 2010, 2015; Wimble-
don et al. 2013; Svobodová Koš ák 2016). An opening of
the Tethyan/Panthalassa passage between Gondwana and
North America enabled phyletic evolution of small plank-
tonic protozoans and autotrophic algae in a renewed circum-
equatorial oceanic current. This evolution led to a high

MICHALÍK, REHÁKOVÁ, GRABOWSKI, LINTNEROVÁ, SVOBODOVÁ, SCHLÖGL, SOBIE and SCHNABL

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number of bioevents useful for global correlation of pelagic
carbonate sequences. In spite of their broad spatial extent,
these events differed in details due to regional palaeoenvi-
ronmental changes (Michalík & Reháková 2011). We think
that the boundary level should be situated within a bundle of
such events, allowing good correlations in the absence of the
primary ammonite markers.

The warming in combination with eustatic oscillations

could result in diverse changes of the fauna in the Panboreal
Realm (Wimbledon et al. 2013; Zakharov et al. 2014). During
prominent sea-level rise, connection of the Boreal sea with
the Panthalassa Ocean opened as indicated by occurrences of
Middle Volgian ammonites with Pacific affinity. Disturbance
of the marine ecosystem indicated by green algae blooms
correlates with a negative excursion of C

org

isotope near the

Volgian/Ryazanian boundary. The stratigraphic correlation is
difficult between the Boreal and Tethyan bioprovinces
because they underwent different evolutionary pathways, the
only connecting link seems to be the magnetostratigraphy
(Houša et al. 2007; Grabowski 2011; Schnabl et. al. 2015).

Our paper discusses the results of an integrated biostrati-

graphic study using three microplankton groups (calpionel-
lids, calcareous dinoflagellates and nannofossils), stable iso-
tope data (

O), microfacies and sequence stratigraphy,

as well as the study of magnetic record in the Strapkova sec-
tion, which is regarded here as an auxiliary West Carpathian

regional JKB section. The
distribution of the strati-
graphi cally-important plank-
tonic organisms revealed
se

veral coeval calpionellid

and nannofossil bioevents
recorded in the pelagic car-
bonate sequence of the JKB.
The bioevents can be inte-
grated with magnetostratigra-
phy. In addition, magnetic
susceptibility helps us to
interpret early depositional
history of the sediment,
namely the amount of supply
of fine-grained terrigenous
material to a basin.

Location of the studied

sections

An important section

exposing the JKB sequence in
the western sector of the Pie-
niny Klippen Belt (Western
Carpathians, Slovakia) is
named the Strapkova section
(Fig. 1). It can be well cor-
related with the principal

Brodno section that is located about 40 km NE of the Strap-
kova section. Two additional JKB sections studied in detail
(Strá ovce and Hlbo a) are located in the Krí na Nappe of
the Central Western Carpathians (Michalík et al. 1995;
Grabowski et al. 2010). The Strapkova section
(49°04’09.34”N; 18°10’00.85”E; 589 m a.s.l.) is exposed on
a steep SE slope of the Strapkova hill below the Mount
Vršatec (Biele Karpaty Mountains, Fig. 1). It is located below
a local road leading from Vršateck  Podhradie to  erven
Kame , approximately 1250 m NE from the Vršateck
Podhradie village, westwards of the middle Váh Valley. The
Brodno section (49°16’02.16”N; 18°45’12.16”E; 353 m a.s.l.)
has been described by Houša et al. (1996), Michalík et al.
(1990, 2009) as the parastratotype section of the JKB in the
Western Carpathians. It is situated in an abandoned quarry
north of  ilina town on the eastern side of the narrow straits
of the Kysuca River Valley (known as the “Kysuca Gate”).

Geological setting

The tectonic contact of two principal superunits of the

Western Carpathians (the Outer and Central Carpathians) is
rimmed by the Pieniny Klippen Belt (Fig. 1). This unit, ori-
ginally rimming the European shelf, is typical of tensional
basins-and-ridges development from the Early Jurassic until

Fig. 1. A — Situation sketch of the studied area (gray ellipse) in the frame of Slovakia (arrow indicates
the Hlbo a section); B — Situation sketch of the Middle Váh Valley section of the Pieniny Klippen
Belt with indication of the Brodno and Strapkova sections (arrows). — Simpli ed geological sketch
of the Pieniny Klippen Belt area between erven Kame , Prusk and Krivoklát villages.

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the Palaeogene, not interrupted by Palaeoalpine tectonic
movements, when the superficial nappe structure of the Cen-
tral Carpathians originated. Its typical klippen-style tectonic
contrasts with a slight diagenetic transformation of its rock
sequences. In contrast to the Pieniny Klippen Belt, sedimen-
tary rocks of Central Carpathian sequences are more strongly
affected both by diagenesis and tectonic stress. This weak
degree of diagenetic transformation thus favours a complex
study of the Jurassic and Cretaceous sedimentary sections in
the Pieniny Klippen Belt. They formed in two parallel shal-
low, but considerably subsiding marine basins separated by
the Czorsztyn Ridge. The Strapkova and Brodno sections
formed in more distal areas of the Kysuca Basin, in the
neighbourhood of the Penninic rift system, which was gra-
dually invaded by the Mid Atlantic-Penninic Ocean arm
during the Jurassic and Cretaceous (Michalík 1994; Plašienka
2003).

Hemipelagic succession of the Strapkova section

(attributed to the Orava Unit by Haško 1978 and Schlögl et
al. 2000; Fig. 2) starts with the Lower Jurassic spotted lime-
stones. An ammonite fauna indicates the Late Sinemurian
Raricostatum Subzone. The Kozinec Formation composed of
red pseudonodular limestones alternating with greenish-grey
marly limestones contains ammonites spanning the latest
Sinemurian Macdonelli Subzone of the Raricostatum Zone
up to the Early Pliensbachian Davoei Zone. Grey-greenish
finely bedded limestones and yellow-grey marly shales con-
tain abundant ammonites of the Pliensbachian and Toarcian
Margaritatus and Spinatum zones. Red nodular limestones
following upwards are considered Toarcian in age. Well-
bedded cherty spiculitic limestones of the Podzamcze Lime-
stone Formation contain isolated beds of crinoidal pack-
stones, capped by a 1 m thick interval of red nodular lime-
stone (Fig. 2). The Czajakowa Radiolarite Formation is built
of red radiolarites (1 m thick) with Middle Oxfordian radio-
larians, a thick (1.5 m) layer of pink limestone rich in belem-
nite rostra and “upper” red and green radiolarites with Kim-
meridgian Saccocoma packstones in its upper part. Radiola-
rites pass gradually into thin bedded red cherty and nodular
limestones intercalated by red marlstones. The marlstones
are followed by the Czorsztyn and the Pieniny limestone for-
mations, which formed the subject of our study.

Methods

Microfossil and microfacies study

88 limestone beds have been sampled for thin sections.

Beds have been numbered (mostly at 1 metre intervals) by
numbers from 279 to 382 in accordance with former sam-
pling (Schlögl 2001) of the entire section. The interval 301 to
324 has been omitted due to uncertainties connected with
slump deformation. According to new analyses, it seems that
distortion of original thickness is not significant. More
densely sampled intervals (around the JKB) have been

designated according to a decimal system. Pure limestones
without cherts and silicified parts were selected for thin-
sections. The majority of samples have been analysed also
for stable isotopes (C, O), carbonate and TOC content.

A set of 110 samples was used for microfacies analyses in

order to document the succession of calpionellids and calca-
reous dinoflagellates. The thin-section samples were studied
under the LEICA DM 2500 transmitting light microscope
and the percentages of selected allochems and bioclasts
(quartz and lithoclasts, calpionellids, radiolarians, globo-
chaetes, saccocomids, filaments, clasts of benthic organisms)
were calculated. The quantitative evaluation with the optical
charts sensu Bacelle & Bosellini (1965) was used. Microfa-
cies and biostratigraphically-important microfossils were
documented using a LEICA DFC 290 HD camera. Thin-
sections are stored in the collections of the Earth Science
Institute of the Slovak Academy of Sciences and in the col-
lections of the Department of Geology and Palaeontology
(Faculty of Natural Sciences), both in Bratislava.

Calcareous nannofossils were analysed in 99 smear slides

prepared using technique reported by Švábenická (2012) —
decantation method and 7 % solution of H

. To obtain the

relative sample abundances and semi-quantitative informa-
tion about nannofossil species, all the specimens in at least
300 fields of view were counted in each slide. The smear
slides were examined under the Olympus BX51 transmitting
light microscope using an immersion objective of ×100
magnifications. Calcareous nannofossils were documented
with the Olympus DP70 digital camera. The set of smear
slides is stored at the Department of Geology and Palaeonto-
logy, Faculty of Science (Charles University, Prague) and at
the Institute of Geology of the CAS in Prague.

Geochemistry

Stable isotopes (C, O) and total carbon (TOC) analyses

were carried out on bulk rock carbonate samples. 64 samples
were selected to C and O isotope analyses: 31 samples were
selected in the uppermost Jurassic to the JKB interval (281–
300 M) and the next 33 samples were taken in the Berriasian
(325–360 M) interval.

C and

O were analysed in CO

after standard decay of bulk rock samples in 100 % phos-
phoric acid. Analyses of carbonate samples were done in
labo ratories of the Czech Geological Institute in Prague on
the Finigan MAT-2 Mass Spectrometer and in the Earth
Science Institute of the Slovak Academy of Sciences in
Banská Bystrica on the MAT253 Mass Spectrometer
equipped with the Gasbench device (Thermo Scientific Sam-
ples). Results are introduced in standard del-notation ( ) in
promile (‰) being related to the Vienna Pee Bee Belemnite
(VPDB) standard with 0.01 ‰ accuracy.

The palaeotemperature calculation from calcite oxygen

isotopes (Anderson & Arthur 1983) is as follows:
T(°C) 16.0–4.14(

–

)+0.13(

–

)

, where

O of

calcite of samples in ‰ (V-PDB) and

O of sea water.

According to Gröcke et al. (2003), the value –1.0 ‰

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(V-SMOW) is characteristic of the post-Jurassic ice-free
world. The contents of total organic carbon (TOC) and total
inorganic carbon (TIC) were detected in 50 bulk rock sam-
ples on the C-MAT 5500 device of the Ströhlein Firm in the
Earth Science Institute of the Slovak Academy of Sciences in
Banská Bystrica. The TIC content was re-calculated on
CaCO

contents.

Palaeomagnetism and magnetic properties

65 stratigraphic layers were sampled for a magnetostrati-

graphic study between beds 292 and 364. Samples were
taken either with gasoline or electrically powered drills.
Sampling resolution was usually 0.5–1 m. Standard cylindri-
cal specimens 2.2 cm high and 2.5 cm in diameter were pre-
pared from drill cores. Usually, at least two twin specimens
were obtained from each drill core. The first specimen was
subjected to thermal demagnetization and palaeomagnetic
analysis, and the second one was used for rock magnetic
analysis. Palaeomagnetic experiments were performed in the
Palaeomagnetic Laboratories of the Polish Geological Insti-
tute-NRI in Warsaw and Institute of Geology, Czech Aca-
demy of Sciences in Prague (Pr honice). In the Palaeomag-
netic Laboratory of the PGI-NRI natural remanent magneti-
zation (NRM) was measured with the JR6a spinner magne-
tometer. Specimens were demagnetized exclusively by the
thermal method using the MMTD1 non-magnetic oven
(Magnetic Measurements, UK, rest field <10 nT). Magnetic
susceptibility was monitored with a KLY-2 bridge (AGICO,
Brno; sensitivity 10

-8

SI) after each thermal demagnetization

step. NRM measurements and demagnetization experiments
were carried out in the magnetically shielded space (a low-
field cage, Magnetic Measurements, UK, which reduces the
ambient geomagnetic field by about 95 %). The thermal
demagnetization was also performed in the Institute of Geo-
logy CAS using the MAVACS apparatus, the NRM was mea-
sured on the SQUID magnetometer 2G enterprises 755 4K
SRM with shielded entrance. The magnetic susceptibility
was measured on KLF4 magnetic susceptibility meter from
AGICO. The measured data from both laboratories are fully
compatible.

Results of measurements were further processed using the

Remasoft software (Chadima & Hrouda 2006). Rock mag-
netic investigations were performed in the palaeomagnetic
laboratory in Prague. They comprised mass-normalized mea-
surements of the MS and isothermal remanent magnetization
(IRM). The IRM was applied along the Z axis in the field of
1T, and then antiparallel in the field of 100mT (using
MMPM10 pulse magnetizer). The S-ratio (IRM

100mT

/IRM

)

calculated as ratio of IRM intensities applied in both fields
was indicative for proportions of low and high coercivity
minerals. In samples from selected beds, a stepwise acquisi-
tion of the IRM (in the maximum field of 1.4T) was per-
formed, followed by thermal demagnetization of three axes
IRM acquired in the fields of 1.4T, 0.4T and 0.1T (Lowrie
1990) in order to identify magnetic minerals.

Results

Sedimentology and microfacies

The

(ca. 11 m thick,

samples 280 to 291, Fig. 2) is represented by red nodular
limestones of the Ammonitico Rosso facies. Ammonites are
affected by corrosion and dissolution and thus are very poorly
preserved. The formation includes Saccocoma-filamentous
wackestones to packstones, Saccocoma-Globochaete-fila-
mentous packstones, Saccocoma-radiolaria-Globochaete
packstones,  Saccocoma-Globochaete-radiolaria packstones,
Saccocoma-Globochaete wackestones to packstones (Fig. 3),
and radiolarian wackestones. In addition to dominant bio-
clasts, they contain rare aptychi, crinoids (formed by twinned
lamellar calcite), echinoids, juvenile ammonites, calcitic and
agglutinated foraminifera, thick-walled bivalves, sponge
spicules, the problematicum Gemeridella minuta, and calca-
reous dinoflagellate cysts. Dinocysts are represented by
Cadosina parvula, Colomisphaera nagyi,  Stomiosphaera
moluccana,  Carpistomiosphaera borzai,  Colomisphaera
pulla,  Carpistomiosphaera tithonica (Fig. 4 A),  Colomi-
sphaera radiata (Fig. 4 A),  Colomisphaera  carpathica
(Fig. 4 C),  Colomisphaera lapidosa,  Parastomiosphaera
malmica, Cadosina semiradiata fusca (Fig. 4 D), and Cado-
sina semiradiata semiradiata  (Fig. 4 E).  Radiolarians and
spicules are partially or totally calcified. Nodules are rimmed
by dense systems of stylolites. Silt-sized muscovite flakes
and quartz grains are common locally, and concentrated in
the dissolution zones of stylolites. The matrix contains scat-
tered pyrite aggregates. Saccocomas dominated in the Kim-
meridgian and Lower Tithonian associations (Figs. 2, 3).
Since the Late Tithonian, they were gradually replaced by
Globochaete alpina spores.

The

is formed by pale

grey to white biomicritic limestones, with variable bed thick-
ness. Radiolaria-Globochaete-calpionellids, radiolarian-
calpionellid-Globochaete, Globochaete-Calpionella and
calpionellid-Globochaete-nannofossil microfacies were
identified. The abundance of bioclasts in micrite matrix
varies between wackestone to packstone (Fig. 5). The lime-
stones contain numerous calpionellids, foraminifera, Invo-
lutina sp. Lenticulina sp., benthic and planktonic crinoid seg-
ments (Saccocoma sp.), echinoids, ophiuroids, bivalves,
juvenile ammonites, aptychi, ostracods, sponge spicules,
problematicum Didemnoides moreti, and Didemnum carpa-
ticum. Local silty quartz grains and scattered (also framboi-
dal) pyrite occur in the matrix (Fig. 3B–F). Layers con taining
sedimentary breccia and synsedimentary slumps were
observed locally.

Biomicrite wackestone of radiolarian-calpionellid micro-

facies (in 29 beds, samples from 298 to 339), contains almost
the same bioclasts as those observed in the Crassicollaria
Zone. Saccocomids disappeared (Fig. 5); crassicollarian lori-
cas are currently deformed. Small bioclasts are sometimes
affected by silicification; phosphatization of fragments was

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Fig. 3. Microfacies in the Strapkova section: A — Saccocoma packstone. Sample 287. B — Aptychi
and crinoid fragments in Calpionella-Globochaete wackestone to packstone. Sample 296.3.

— Slightly bioturbated Calpionella-Globochaete packstone. Sample 296.3. D — Biomicrite radio-

laria-calpionellid and Calpionella-Globochaete wackestone. Samples 298; 298.5. E — Biomicrite
radiolarian wackestone. Sample 300. F. Biomicrite Calpionella wackestone. Sample 300.2.

Depositional environment
and sequence architecture

The wackestones and pack-

stones of the Pieniny Lime-
stone Formation are formed
mostly by tests of planktonic
microorganisms, while mud-
stone micrites and biomicrites
consist of nannoplankton
remains and unidentified cal-
cite test fragments. Although
stratigraphic differences in
the rock composition and in
the granulometry of the “bian-
cone” facies are not exten-
sive, eight 7–16

m-thick

cycles can be distinguished in
the sequence (Fig. 2). Each of
the cycle starts with pack-
stone beds containing infre-
quent remnants of benthic
organisms, abundant (some-
times redeposited) tests of
calpionellids, occasional small
(eolian) grains of quartz and
mica leaflets. These beds are
comparable with the lowstand
part of the cycle. Upwards,
limestone beds are characteri-
zed by a higher content of cal-
careous dinocysts and calpio-
nellid tests. The highest part is
richer in chert and frequently
includes laminar concentra-
tions of (mostly calcified)
radiolarian tests. These cycles
correspond to the eustatic
cycles (Ti3-Ti6 and Be1-Be4)
figured in Haq (2014).

The distribution of calpio-

nellids shows several abundance peaks (Figs. 2, 5). The first
peak is located in the Late Tithonian, the second peak is
located in the upper part of the Alpina Subzone, and the third
peak is located below the onset of the Ferasini Subzone.
Stratigraphic changes in abundance of calpionellids and radio-
larians (Figs. 2, 5) show that they alternate in discrete peaks:
a decrease in abundance of calcareous plankton is associa ted
with an increase of abundance of silica-secreting organisms
(Reháková & Michalík 1994; Michalík et al. 2009).

Locally,

bioclasts are accumulated in thin laminae and small nests,
some of bioclasts that are slightly phosphatized.

Radiolarians occur in very thin silicified laminae at multiple

levels (I samples 315.15; 333; 339, 351.1; 381.9; 385.8;
388.25; 388.6; 393.2; 394.3; 395.15) that can be interpreted
as contourites (Schlögl et al. 2000). These laminites

observed more rarely. Clastic admixture is represented by
rare eolian silty quartz grains only (Fig. 2).

Silty clastic admixture content (quartz and muscovite in

samples 340 to 359) is low (Fig. 2). Some layers contain
lami nae rich in bioclasts. Pyrite is scattered in matrix, it
occurs as framboids or in nest accumulations. Several bio-
clasts, mainly radiolarians are impregnated by pyrite, some
other bioclasts were phosphatized.

The sampling of the sequence has been complicated in the

two sections in which the stratal geometry is distorted by
folds (between 300–325, and 347–346). Study of sedimen-
tology, and detailed biostratigraphy indicates that these
phenomena originated synsedimentary due to rock sliding.
Their presence confirms the slope environment of
sedimentation.

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Fig. 4. Calcareous dinocysts in the Strapkova section: A — Carpistomiosphaera tithonica Nowak.
Sample 287. B — Colomisphaera radiata (Vogler). Sample 287.   — Colomisphaera carpathica
(Borza). Sample 287. D — Cadosina semiradiata fusca (Wanner). Sample 290. E — Cadosina semira-
diata semiradiata (Wanner). Sample 290. F, G — Colomisphaera fortis  ehánek. Samples 290; 298.3.
H — Colomisphaera cieszynica Nowak. Sample 300.3. I — Colomisphaera lapidosa (Colom). Sam-
ple 300.3. J — Stomiosphaerina proxima  ehánek. Sample 300.3. K — Gemeridella minuta Borza et
Mišík. Sample 300. L — Didemnum carpaticum Borza et Mišík. Sample 300.1.

represent a special feature of
the Strapkova sequence (Fig. 6).
The abundance of radiolarian
tests is the highest in each
fifth

lamina (1.9 to 2.2 mm

thick) with a slightly erosive
base. Similar limestone layers
with radiolarian laminae
occur in the Brodno (Michalík
et al. 2009; bed C42) and
Rochovica sections (in the lat-
ter case, they occur in much
younger, Valanginian to Aptian
strata; Michalík et al. 2008).

The layer below the radio-

larian laminite is bioturbated
(Fig. 6A–C). Traces of Chon-
drites,  Palaeophycus,  Plano-
lites,  Thalassinoides, and
Trichichnus were identified in
cross-sections perpendicular
to the bedding plane. Primary
sedimentary features (cross-
bedding stratification, lamina-
tion) were mostly destroyed
by bioturbation. The largest
burrows (Thalassinoides) are
on average 5–9 mm in diame-
ter, Planolites and Palaeophy-
cus burrows attain diameters
of 2 to 3 mm. Planolites and
Thalassinoides burrows are
pe netrated  by Chondrites (with
diameters of 0.4 to 0.6 mm).
Simple vertical pyritic bur-
rows of Trichichnus are
0.2 mm in diameter. Framboi-
dal pyrite clusters co-occur in
places with bioturbation
structures. The size of bur-
rows, different ethological
character (domichnia, fodi-
nichnia, chemichnia) and tro-
phic levels of these traces
indicate that the bottom was
well supported with nutrients
and oxygen, and inhabited by
burrowers at different sediment depths.

Biostratigraphy

Calpionellid and calcareous dinocyst zonations

Red nodular limestone of the Rosso Ammonitico facies

(Czorsztyn Limestone Formation) is dated as late

Kimmeridgian (Borzai and Pulla zones) to latest Early Titho-
nian Chitinoidella boneti Subzone (Jach et al. 2012). The
succession of dinoflagellate bioevents allowed us to deter-
mine the following dinocyst zones: the Late Kimmeridgian
— Borzai (sample 280) and Pulla zones (samples 281–283),
and the Early Tithonian — Malmica Zone (samples 284 to
287). After a thin transitional interval (earliest Late Tithonian
Praetintinopsella Zone), the sequence continues with the
Maiolica facies of the Pieniny Limestone Formation (Late

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Tithonian to late Berriasian). Our study has been focused on
the lower part of the Pieniny Formation, ca. 40 m thick (from
the Late Tithonian Crassicollaria remanei Subzone to middle
Berriasian Calpionella elliptica Subzone). Successive occur-
rence of biostratigraphically important calpionellids and cal-
careous dinoflagellates is shown in the Fig. 7.

(sensu Grandesso 1977 and Borza 1984)

Saccocoma-Globochaete-radiolaria packstones (samples

288 to 289) contain rare Longicollaria  dobeni (Fig. 8A)
Carpathella rumanica,  Borziella slovenica, Dobeniella
tithonica,  Colomisphaera  carpathica,  Colom. lapidosa and
Colom. tenuis.

(sensu Grandesso 1977 and Borza 1984)

Saccocoma-Globochaete-radiolaria packstones and Sacco-

coma-Globochaete  wackestones to packstones (samples
289.4–290) with Chitinoidella boneti (Fig. 8B), Chitin. elon-
gata  (Fig. 8C), Longicollaria  dobeni,  Dobeniella cubensis,
Popiella oblongata,  Colomisphaera  carpathica,  Colom.
lapidosa, Colom. tenuis and Colom. fortis (Fig. 4F, G).

(sensu Grandesso 1977)

Radiolaria wackestones (sample 291) contain rare chiti-

noidellids, cysts of Colomisphaera carpathica but also the
first hyaline calpionellid form represented by Praetintinnop-
sella andrusovi (Fig. 8E).

(sensu Remane et al. 1986)

Radiolarian wackestone (sample 293) with very rare sec-

tions of microgranular chtitinoidellids contains Tintinopsella
remanei (Fig. 8D), Calpionella alpina, Crassicollaria inter-
media, and cysts of Colomisphaera carpathica.

(sensu Remane et al. 1986)

Calpionella-Globochaete locally slightly laminated wacke-

stones to packstones (8 beds from 294 to 294.6) with Crassi-
collaria intermedia (Fig. 8F), Crass. parvula, Crass. massu-
tiniana (Fig. 8G), Calpionella alpina, Calp. grandalpina
(Fig. 8K), Calp. elliptalpina, Tintinnopsella carpathica, and
cysts of Colomisphaera lapidosa, Colom. carpathica,
Stomio sphaerina proxima, Cadosina semiradiata semiradiata,
and Cadosina sp.

(sensu Reháková & Michalík 1997)

Radiolarian-Calpionella-Globochaete, Calpionella-Globo-

chaete, Globochaete-Calpionella, locally slightly laminated
and/or bioturbated wackestones (18 beds from 294.7 to
296.2) contain Crassicollaria brevis (Fig. 8H), Crassicol-
laria parvula, Calpionella alpina; Crassicollaria massuti-
niana, Calpionella grandalpina, Tintinnopsella carpathica,
cysts of Colomisphaera lapidosa, Colomisphaera carpathica,
Stomiosphaerina proxima, Cadosina semiradiata semiradiata
and Cadosina semiradiata fusca are less abundant if com-
pared with the Intermedia Subzone.

(sensu Reháková & Michalík 1997)

The FO of Crassicollaria colomi was identified in slightly

bioturbated biomicrite (16 beds from 296.3 to 297) with
Calpionella-Globochaete  (Fig. 3B, C), radiolarian-Calpio-
nella, radiolarian-Calpionella-Globochaete and radiolarian
microfacies.  Crassicollaria parvula dominates over Crass.
colomi  (Fig. 8I), Crass. brevis,  Crass. massutiniana, and
Calpionella alpina (Fig. 8J), which prevails over Calpionella
grandalpina and Tintinnopsella carpathica. Colomisphaera
lapidosa, Colom. carpathica, Stomiosphaerina proxima,
Cadosina semiradiata semiradiata, Cados. semiradiata
fusca cysts were also identified.

(sensu Pop 1974; Remane et al. 1986;

Reháková & Michalík 1997; Lakova et al.1999;

Boughdiri et al. 2006; Andreini et al. 2007;

Lakova & Petrova 2013).

Fig. 6. Bed 393.1 of the maiolica limestone with accumulations of
radiolarian tests arranged in laminae (A, the uppermost part). Under-
lying rock is penetrated by burrows of infaunal organisms (B) indi-
cating more intensive oxidation (B) of dysoxic sediment by bottom
current. — Another bed (351.1) of the maiolica limestone with
radiolarian tests in distinct laminae deposited from a contour
current.

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Biomicrite wackestone is composed of radiolarian, radio-

larian-calpionellid and calpionellid microfacies (29 beds
between 298–339; Fig. 3E, F). The sample 298 shows transi-
tion from the microfacies rich in Crassicollaria parvula to
microfacies in which spherical forms of Calpionella alpina
dominate. Thus, the J/K boundary interval according to
Remane’s et al. (1986) definition is situated in bed 298. Four
crassicollarian abundance events influenced by synsedimen-
tary erosion were documented (samples 298.1–298.4). Since
the sample 298.6, Calpionella-Globochaete wackestones
prevail (Fig. 3D), radiolarians appear in high portion in sam-
ples 299, 332 and 338. The dominant Calpionella alpina
with rare Crassicollaria parvula and Tintinnopsella car-
pathica with Tint. doliphormis create a calpionellid associa-
tion typical of the Alpina Subzone. Calpionellids are accom-
panied by rare to seldom cysts of Colomisphaera carpathica,
Col. cieszynica (Fig. 4H), Col. lapidosa, (Fig. 4I), Col. cf.

fortis, Col. sp., Stomiosphaerina proxima (Fig. 4J) and
Cadosina semiradiata semiradiata, microproblematica of
Gemeridella minuta (Fig. 4K) and Didemnum carpaticum
(Fig. 4L).

(sensu Remane et al. 1986)

Biomicrites, locally slightly bioturbated with calpio nellid-

Globochaete, calpionellid-Globochaete-radiolarian and
radio larian wackestones (studied in samples 340–343). In the
calpionellid association Calpionella alpina dominated over
the infrequent Remaniella ferasini, R. catalanoi, R. duran-
delgai, R. borzai, Tintinopsella carpathica, Crassicollaria
parvula. The dinoflagellate cyst association consists of Colo-
misphaera lapidosa, Col. carpathica, Stomiosphaerina
proxima, Cadosina semiradiata fusca and Cad. semiradiata
semiradiata.

Fig. 7. Vertical range of calpionellid species and cysts of calcareous dino agellates.

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(sensu Pop 1974)

Biomicrites, locally bioturbated wackestones (samples 344–

359) with radiolarian-Calpionella-Globochaete and Calpionel-
la-Globochaete microfacies contain calpionellid associations
of Calpionella alpina, Calp. elliptica (Fig. 9B, C), Calp.
minuta, Tintinopsella carpathica (Fig. 9L), Tint. longa
(Fig. 9A), Lorenziella hungarica (Fig. 9I), Remaniella catala-
noi, Rem. ferasini (Fig. 9D, E), Rem. durandelgai (Fig. 9F),

Rem. borzai

(Fig. 9 H), Rem.

colomi, Rem. filipescui, Rem.
cadischiana (Fig. 9G). Cysts
are represented by Colomi-
sphaera lapidosa, Colom.
carpathica, Cadosina semira-
diata semiradiata and Cad.
semiradiata fusca.

Calcareous nannofossils and
nannofossil zonation

In the samples studied, cal-

careous nannofossils are
rather rare and their preserva-
tion ranges from moderate
(only in a few samples) to
extremely poor, heavily etched
by dissolution. In total, 29
calcareous nannofossils taxa
were indentified. A compara-
ble diversity has been
observed in the Barlya section
(Lakova et al. 1999) and in
the Nutzhof (Reháková et al.
2009). A slightly lower diver-
sity has been reported from
the Brodno (Michalík et al.
2009) and Hrušové sections
(Ondrejí ková et al. 1993),
conversely higher diversity
and abundance also have been
observed, for example, in the
Puerto Escaño (Svobodová &
Koš ák 2016) or Torre de
Busi and Foza sections
(Casellato 2010). Successive
distribution of nannofossils
along the lithological column
is shown in the Fig.

10.

Watznaueria (more than 55 %),
Cyclagelosphaera (nearly

20 %), Conusphaera (14 %),
and Nannoconus (7 %) are
the most abundant compo-
nents of the assemblage

(Fig. 10). The occurrence of

these most abundant genera is in accordance with previous
studies of calcareous nannofossils of the JKB interval (e.g.,
Michalík et al. 2009; Reháková et al. 2009; Lukeneder et al.
2010; Wimbledon et al. 2013). Nannoliths represented by
Polycostella beckmannii, Hexalithus noeliae and Assipetra
infracretacea are less present. The species indicative of
eutrophic environments such as Zeugrhabdotus erectus and
Diazomatholithus lehmannii occur only sporadically. Despite
the poor preservation, several biostratigraphically important

Fig. 8. Calpionellids in the Strapkova section: A — Longicollaria dobeni (Borza). Sample 288.
B — Chitinoidella boneti Doben. Sample 290. — Chitinoidella elongata ehánek. Sample 289.
D — Tintinnopsella remanei Borza. Sample 293. E — Praetintinnopsella andrusovi Borza. Sample
291. F — Crassicollaria intermedia (Durand Delga). Sample 294. G — Crassicollaria massutiniana
(Colom). Sample 293. H — Crassicollaria brevis Remane. Sample 295. I — Crassicollaria colomi
Doben. Sample 298.1. J — Calpionella alpina Lorenz. Sample 295. K — Calpionella grandalpina
Nagy. Sample 294. L — Tintinnopsella carpathica (Murgeanu and Filipescu). Sample 347.

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species have been recorded: Nannoconus wintereri, N. stein-
mannii minor, N. kamptneri minor, N. steinmannii stein-
mannii. The full list of calcareous nannofossil taxa found is
given in alphabetical order in the “Appendix” and strati-
graphically important taxa in the Fig. 11.

The abundance of calcareous nannofossils in the sequence

is generally low. On average throughout the section, about
50 specimens per sample were observed. It means one speci-
men per six fields of view of the microscope. Due to the low
abundance and prevailing bad preservation of calcareous
nannofossils, only several biostratigraphic events have been
defined. The first occurrence (FO) of N. wintereri was
recorded in the bed 298.1, close to the expected JKB interval
based on calpionellids (this study, see above). This bioevent
represents the base of the NJT 17b Subzone, which Casellato
(2010) considered to cover the JKB interval. The FO of
N. steinmannii minor was recorded in bed 300.0 in middle
part of the M19n magnetozone. Casellato (2010) indicates it
as the base of the NKT Zone. N. kamptneri minor occurs spo-
radically from bed 343 upwards. The FO of N. steinmannii
steinmannii, namely the base of the NK-1 Zone sensu

Bralower et al. (1989) was
recorded in bed 352, in the
lower part of the Elliptica
Subzone (Fig. 10). N. kampt-
neri kamptneri was not found
in the samples studied.

Geochemistry

Carbonate and C

org

contents

The CaCO

content in the

uppermost part of the Czorsz-
tyn Fm. is relatively high
(Fig.12). In the basal part of
the Pieniny Fm. (from the
beds 291 to 300) it decreases
below 80 %. The decrease is
in accordance with microfos-
sil analysis which pointed to
raised silica bioproduction.
The CaCO

content reaches

up to 90 % again in the Pieniny
Fm. (325–360), where nanno-
conid and calcareous micro-
plankton remnants become
abundant (Tremolada et al.
2006; Michalík et al. 2009;
Grabowski et al. 2013).

However, locally — as in

bed 334 (Fig. 12), the CaCO

content decreases below
50 %. Microfacies study have
suggested that the main

source of silica in the whole sequence came from radio larians
and only a very low amount came from detrital minerals
(quartz, clays, accessories; Figs. 2 and 5). Silica (opal–
chalcedony) came from radiolarian tests, replaced by calcite
and concentrated in cherts.

TOC content is low (0.08–0.31 %) in all samples (Fig. 12).

The C

org

contents slightly increases (more than 0.1 %) in the

top of the Czorsztyn Fm and at the base of the Pieniny Fm.,
where CaCO

content decreases. Similarly, in beds 350 and

353, slight TOC accumulation could result from selective
sorption of (dissolved) C

org

by fine grains with more active

surface, but probable also from raised fossil production.

Stable carbon and oxygen isotopes

Both C and O isotopes of bull rock samples show a rela-

tively small variation and shift within a relatively narrow
range (

C range from +1.09 to +1.96 ‰ VPDB,

O from

–2.93 to –1.20 ‰ VPDB). Late Tithonian

C values (+1.96

to +1.46 ‰ VPDB) show a slightly decreasing trend
(Fig. 12). Next, higher up section (beds 188–300) values

Fig. 9. Calpionellids in the Strapkova section: A — Tintinnopsella longa (Colom). Sample 345.

— Calpionella elliptica Cadisch. Samples 344; 359. D, E — Remaniella ferasini (Catalano).

Sample 346; 354. F — Remaniella durandelgai Pop. Samples 344; 346. G — Remaniella cadischiana
(Colom). Sample 359. H — Remaniella borzai Pop. Sample 353. I — Lorenziella hungarica Knauer
and Nagy. Sample 343.

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Fig. 11. Important nannofossils species. Scalebar represents 5 μm. A — Watznaueria barnesiae (Black in Black & Barnes) Perch-Nielsen.
Sample 291. B — Watznaueria manivitiae (Bukry) Moshkovitz & Ehrlich. Sample 330. — Watznaueria britannica (Stradner) Reinhardt.
Sample 299.5. D — Cyclagelosphaera margerelii Noël. Sample 293. E — Cyclagelosphaera

(Manivit) Roth. Sample 300.1.

F — Diazomatolithus lehmanii Noël. Sample 297.3. G — Hexalithus noeliae (Noël) Loeblich & Tappan. Sample 299.4. H — Conusphaera
mexicana (Trejo) subsp. minor (Bown and Cooper) Bralower in Bralower et al. Sample 295. I — Conusphaera mexicana (Trejo) subsp.
mexicana Bralower in Bralower et al. Sample 299.3. J — Zeugrhabdotus embergeri (Noël) Perch-Nielsen. Sample 298.4. K — Nannoconus
globulus (Brönnimann) subsp. minor Bralower in Bralower et al. Sample 330. L — Nannoconus globulus (Brönnimann) subsp. globulus
Bralower in Bralower et al. Sample 350. M — Nannoconus wintereri Bralower and Thierstein in Bralower et al. Sample 352. N — Nanno-
conus kamptneri (Brönnimann) subsp. minor Bralower in Bralower et al. Sample 356. O — Nannoconus steinmannii (Kamptner) subsp.
minor Deres and Achéritéguy. Sample 300. — Nannoconus steinmannii (Kamptner) subsp. minor Deres and Achéritéguy. Sample 300.
Q — Nannoconus steinmannii (Kamptner) subsp. minor Deres and Achéritéguy. Sample 381. R — Nannoconus steinmannii (Kamptner)
subsp. steinmannii Deres and Achéritéguy. Sample 358.

achieving a range of +1.14 to +1.38 ‰ (in average +1.24 ‰
VPDB) show a new (balanced) isotope C composition of
marine water during sedimentation of the Pieniny Fm. The
high resolution carbon isotope record resembles the typical
(stable or smooth) trend worldwide documented in the J/K
boundary sequence (Weissert & Mohr 1986; Weissert &
Channel 1989; Weissert & Lini 1991; Gröcke et al. 2003;
Tremolada et al. 2006; ák et al. 2011; Price et al. 2016). The
same

C values between +1.3 to +1.5 ‰ (VPDB) occur in

the Brodno (+1.3 to +1.6 ‰), Hlbo a (+1.0 to +1.5 ‰), and
Strá ovce (+1.0 to +1.3 ‰) sections (Michalík et al. 1995;
2009). At the Nutzhof section that was also located on the
north Tethyan margin (Lukeneder et al. 2010) which is in an
equivalent position on the north Tethyan margin, bulk carbon
isotope values range between +0.49 and +2.10 ‰.

The range of

O data is not larger than 2 ‰,

O values

are relatively high in nodular limestones of the Czorsztyn
Formation, and sharply decline at the onset of the Middle
Tithonian. However, on average they remain close to 2 ‰
VPDB in the Pieniny Formation (Fig. 12). Although

values strongly vary over small stratigraphic scales, namely
between individual beds, they do not show clear large-scale
trends.

O values can be diagenetically modified more

strongly than

C. In the basal part of the Pieniny Fm (beds

292–300.6)

O data shift from –1.48 to –2.48 ‰.

values in higher part of the section (325–360) reach –1.84 to
–2.93 ‰.

Rock magnetism and demagnetization

Samples were moderately to weakly magnetic with NRM

intensities in the lower part of the section (up to sample 335
including Tithonian and lower part of the Berriasian) mostly
between 1 and 5×10

-4

A/m. Sample 296.5 revealed the high-

est NRM intensity around 9.5×10

-4

A/m. Higher up, in the

upper part of the lower Berriasian, the NRM values fluctu-
ated around 1×10

-4

A/m (Supplementary Fig. S1).

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Low coercivity minerals dominate within the section

which is manifested by negative values of S-ratio, mostly
between –0.9 and –0.7 (Supplementary Figs. S1 and S2).
Three samples (ST 333, 337.5 and 356.5) reveal slightly
higher values of S-ratio: between –0.5 and –0.3. A single
sample ST 296.5 reveals an extremely high value of S-ratio:
0.54. The sample 296.5 also contains an unusually large
amount of ferromagnetic minerals which is manifested by
a very high intensity of the IRM

(Supplementary Fig. S1).

The sample 296.5 might also be distinguished by relatively
high unblocking temperatures (up to 620

C) and slightly dif-

ferent direction of C component (see below). Results of Low-
rie’s (1990) analyses (Supplementary Fig. S3A) confirm that
medium and high coer

civity minerals dominate in this

sample. The maximum
unblocking temperature of
640

C unambiguously indi-

cates the presence of hema-
tite. Samples with moderately
negative values of S-ratio
(between –0.3 and –0.7)
reveal presence of magnetite
which is a dominant magnetic
carrier. Its presence is docu-
mented by the maximum
unblocking temperature of
520–560

C in the 0.1T curve.

However, the contribution of
hematite is still significant as
can be seen on the 1T curve
(Supplementary Fig. S3B–D).
Samples with low negative
values of S-ratio contain
almost exclusively magnetite
(Supplementary Fig. S3E).

might be observed from the
vertical log of S-ratio (Sup-
plementary Fig. S1) that the
contribution of hematite is
slightly more distinct in the
lower half of the section.

During thermal demagneti-

zation, three characteristic
NRM components were
revealed. The least stable
A

component is unblocked

between 20 and 150–200

(Fig. 13). An intermediate
B

component is demagne-

tized in the temperature range
200–420

C. Finally, a double

polarity C component might
be identified between 420 and
480–520

C. Unfortunately,

abrupt MS rise is observed
during thermal treatment

between 400 and 450

C (Fig. 13) and sometimes the C com-

ponent cannot be demagnetized to the origin.

Age of magnetization components and palaeotectonic
implications

The A component clusters match better in the present day

coordinates (Table 1 and Fig. 14A). Their direction in geo-
graphic coordinates is close to the present day normal pola-
rity geomagnetic field direction in the area of investigation.
Therefore, they are interpreted as recent viscous remanent
magnetization of no geological importance. The mixed pola-
rity component is interpreted as the primary one. After
bedding correction, the normal (Cn) and reversed (Cr)

Fig. 12. Late Jurassic and Early Cretaceous C and O isotope stratigraphy calibrated against quantity of
selected groups of microfossils and siliclastics.

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directions cluster in the NW and SE quadrant, respectively,
of a stereonet with moderate inclination (Fig. 14C). Its pri-
mary nature is also supported by the fact that polarity changes
of the C component correlate well with the Global Polarity
Time Scale (see below). The clustering of the C component
does not improve after tectonic correction (Table 1) as might
be expected in the case of a primary component. The McFad-
den & McElhinny’s (1990) reversal test gives negative results
(critical angle 14.5

30.6

). It might be explained either

by contamination of the intermediate B component or incom-
plete demagnetization of the samples containing hematite.
The B component must be regarded as secondary magneti-
zation, as it always reveals a normal polarity (Fig. 14B). Sig-
nificant spread of both B and C components might result
from overlapping of unblocking temperature spectra and
from incomplete demagnetization of hematite. The position
of the B component is usually close to Cn primary compo-
nent (Table 1). Therefore, the B component most probably
represents pre-folding or early synfolding remagnetization of
normal polarity. It might be acquired during the maximum
burial or early phase of Late Cretaceous folding and thrus-
ting, alike abundant secondary magnetizations documented
in the Central Western Carpathians (Grabowski 2005;
Grabowski et al. 2009).

In the pre-folding coordinates, the declination of C compo-

nent reveals a moderate 46

counter-clockwise (CCW) rota-

tion from the present-day north (Table 1). However, cluster-
ing of the C component is too weak for significant palaeotec-
tonic application (the value of precision parameter k >10 is
required; see Van der Voo 1993). Having applied some selec-
tion (rejecting specimens deviating from the main cluster),
the amount of the CCW rotation slightly decreases to 35

Clustering of the C component (both normal and reversed
populations) improves after tectonic correction, although the
precision parameter k is still slightly below 10 (see Table 1
and Fig. 13d) and the reversal test is still negative. Declina-
tion of the C component is concordant with the general CCW
of the study area. A counter-clockwise rotation of 47

( 18

)

was reported by Márton et al. (2013) from the Upper Creta-
ceous pelagic marls in the PKB in the neighbouring locality
of Vršatec.

Palaeoinclination of the Strapkova sec-

tion (41

), corresponding to palaeolatitude

N 5

is slightly shallower than Titho-

nian–Berriasian palaeoinclinations from
the PKB and Central Carpathian reference
sections (Márton et al. 2015) which results
from incomplete cleaning of the primary
C component.

Magnetostratigraphy and correlation
with the Global Polarity Time Scale
(GPTS)

According to the polarity of the C com-

ponent, four normal (N1–N4) and four

reversed polarity intervals (R1–R4) were documented
(Fig. 15). Samples 292 and 292.5 revealed normal polarity of
the C component (N1 interval). The subsequent four samples
between 293 and 294.5 were of reversed polarity (R1 inter-
val). The long normal polarity (N2) interval was indicated
between 295 and 328.5. It is followed by quick polarity
changes manifested by the R2 (329 and 329.5) and N3 (330)
intervals. The sample 330.5 was of undefined polarity. Three
distinct polarity intervals were distinguished in the upper part
of the section: reversed R3 interval (samples 331.5–334),
normal N4 interval (334.5–341.5) and reversed R4

(343–363.9) interval.

The N1 interval is interpreted as the topmost part of the

M20n magnetozone (Fig. 15). It is situated between the
Tithonian Praetintinopsella Zone and the bottom of the
Remanei Subzone. R1 interval is correlated with the M19r
magnetozone. It covers the Remanei and Intermedia sub-
zones. The long normal N2 interval must be interpreted as
the M19n2n. The boundary between Crassicollaria and
Calpionella zones is usually situated within this magneto-
zone (for review, see Ogg et al. 1991; Grabowski 2011;
Satolli et al. 2015). The short R2 and N3 intervals, in the
lower part of the Alpina Subzone, are respectively correlated
with the M19n1r (“Brodno”) and M19n1n magnetosubzones.
The R3 interval is interpreted as the M18r magnetozone. This
magnetozone is situated entirely within the Alpina Subzone
(Houša et al. 2004; Grabowski & Pszcz kowski 2006;
Pruner et al. 2010). The next normal N4 interval is paralleled
with the M18n. The boundary between the Alpina and Ferasini
subzones falls in the upper part of this magnetozone. It is
concordant with the FAD of Remaniella ferasini which is
observed usually in the M18n magnetozone (Ogg et al. 1991;
Houša et al. 2004). A long reversed R4 interval in upper part
of the section is interpreted as the M17r. It starts in the mid-
dle part of the Ferasini Subzone and continues into the Ellip-
tica Subzone. It is concordant with abundant data from Italian
sections (Ogg et al. 1991) and from the Po rednie sections
(Grabowski & Pszcz kowski 2006), where the FO of
Calpio nella elliptica is observed also in the M17r magneto-
zone. The FO of Remaniella cadischiana is noted in the bed
359 (Fig. 9G). As this taxon usually appears in the upper part

4/62

5.1

13.42

65/-39

9.2

4.9

62/65

308/-42

8.9

5.09

351/73

8.8

5.15

62/65

324/-61

15.3

3.93

321/55

11.1

6.64

30/65

233/52

7.0

13.4

130/-24

10.6

6.33

34/65

Cn+ Cr

213/59

7.6

6.44

314/39

8.5

5.39

64/65

Cn select

324/-62

9.7

10.31

335/55

8.2

14.06

24/65

Cr select

233/55

7.6

13.81

139/-28

8.3

11.82

28/65

Cn+Cr select

205/63

7.6

7.8

6.9

9.16

: Characteristic magnetizations from the Strapkova section. Palaeopoles: (Cn + Cr

population) — Pole latitude: 44.6

N; Pole longitude: 268.2

E; dp 6.0, dm 10.1

(Cn + Cr selected population) — Pole latitude: 52.4

N; Pole longitude: 257.9

E; dp 5.1,

dm 8.4 (dp, dm — con dence oval of palaeopole estimation). Explanations:

— decli-

nation/inclination before tectonic correction,

— declination / inclination after

tectonic correction;

, k — Fisher statistics parameters,

— number of beds inves-

tigated/used for calculation of mean direction.

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of the M17r (Grabowski & Pszcz kowski 2006; Grabowski
et al. 2010), it seems that the top of the section is quite close
to the M17r/M17n magnetozones boundary.

Magnetic susceptibility

There is a moderately good correlation of MS with IRM

(Supplementary Fig. S2A, B). This indicates that there might

be a significant contribution of
ferromagnetic minerals to the
MS. Although a long term
decrease of the IRM

observed as in the case of the
MS (Supp. Fig. S1), the two
curves are not identical which
indicates that the contribution
of paramagnetic minerals to
MS cannot be neglected.

Magnetic susceptibility re

veals a long term decreasing
trend (Supplementary Fig. S1
and Fig. 16). Its values are

relatively high in the lower
half of the section, between
8–16×10

-9

/kg in the Titho-

nian and lowermost Berriasian
(the Alpina Subzone, up to
sample 338). Large MS varia-
tions are also observed in that
part of the section. The MS
decreases by 50 % throughout
the Tithonian, up to the JKB.
Then it fluctuates between

4 and 10×10

-9

/kg in the

lower part of the Alpina Sub-
zone, in M19n and M18r mag-
netozones. Significant increase
up to 12×10

-9

/kg is observed

in upper part of the Alpina
Subzone, in the bottom part of
the M18n magnetozone. Then
MS again decreases through-
out the M18n magnetozone to
4×10

-9

/kg. Within the Fera-

sini and Elliptica Subzones,
MS values gently fall from 4 to
3×10

-9

/kg, with only two

minor positive excursions in
the M17r magnetozone.

Discussion

Environmental proxies

In contrast to other Meso-

zoic system boundaries, the JKB time span was related to
less dramatic environmental changes, generating problems
with the definition of the JKB position, reflected in contra-
dictions of its determination in the Brodno and Strapková
sections (Fig. 17) but also in its definition worldwide
(Lukeneder et al. 2010; Michalík & Reháková 2011;
Wimbledon et al. 2013; Schnabl et al. 2015; Price et al.
2016). Use of complex proxy parameters is inevitable.

Fig 14. Stereographic projections of the magnetization components A, B and C. Left column: before
tectonic correction (in situ); right column: after tectonic correction (in bedding coordinates). Full
symbols – lower hemisphere projection; open symbols – upper hemisphere projection.

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Fig. 17. Integrated correlation of the O and C isotopes curves between Strapkova and Brodno sections.

Fluctuations of O isotope composition and distribution of
nannoliths in “Maiolica-type” limestone, where sedimentary
record, including C isotope composition, has not been
influen ced by clastic input, can closely reflect original envi-
ronmental conditions.

A link between the abundance of calcareous nannofossils

and the CaCO

content can be observed. The calcareous

nanno fossils abundance noticably increases from bed 298.6
and this trend continues up to the bed 299.6. This is an inter-
val with the highest nannofossil abundance in the succession
studied. This peak is associated with a higher CaCO

content

(Figs. 12, 16). Conversely, the lowest calcareous nannofossil
abundance has been recorded in bed 334, with only six speci-
mens. This event correlates with the most remarkable
decrease of the CaCO

content, with the radiolarian event and

with the negative

O excursion (Figs. 12, 16).

The observed shift in the

O values (2 ‰) throughout the

section could indicate a relatively strong temperature change

in the Early Cretaceous ice-free world (Anderson & Arthur
1983; Gröcke et al. 2003; Shurygin et al. 2015) in the JKB
sequence upwards. However, the

O signal can have been

modified by other characteristics of water in the basin and by
diagenetic processes in sediment. Bulk-rock analyses can be
rather informative about relative changes in temperature and
seawater

O composition (Michalík et al. 2009; Lukeneder

et al. 2010, 2015).

The shifts between samples are frequently smaller than

0.5 ‰ (Fig. 12). The first shift that occurred between the top
of the Ammonitico Rosso and base of the Maiolica beds is
relatively large (–1.20 to –2.18 ‰) and could indicate rela-
tively continual and intensive temperature rise by 3.5 to 4
degree over a relative short (185–191 m) interval. The

signal is more stable (–1.48 to –2.15 ‰) at the JKB interval
(192–300.6 m) and suggests stabilization of possible higher
temperature values. Data obtained by detailed study of 25
samples fluctuate in a narrower interval (less than 0.7 ‰)

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do not show any clear trend and imply a stable temperature
regime at the J/KB. Negative

O trend in the Maiolica

sequence (325–360 m) continued and it indicates graded
warming (approx.1–2.5 degree). Similar

O trend and tem-

perature range has been observed in the Brodno (Michalík et
al. 2009) or in the Nutzhof sections (Lukeneder et al. 2010)
or other section ( ák et al. 2011, Price et al. 2016).

Analysis of the data introduced above enabled stratigra-

phical and palaeoecological correlation of the Strapkova and
Brodno sections (Fig. 17).

Bed to bed fluctuation of

coincides with nanno- and microplankton events. During the
Late Tithonian, an increase of Polycostella and Conusphaera
was recorded. Increasing abundance of Nannoconus occurred
during the Early Berriasian. Nannoconid peaks (beds 300;
334; 350–352) correspond to negative

O excursions and

higher calcite accumulation (Fig. 16). Nannoconids are
regarded as warm-water taxa (Street & Bown 2000; Melinte
& Mutterlose 2001; Tremolada et al. 2006; Michalík et al.
2009; Svobodová & Koš ák 2016). According to the O iso-
tope data, changes in calcareous nannofossil assemblage
composition and the appearance of Nannoconus, Polycostella
and Conusphaera (Figs. 10, 16) were followed by warming
of 2–3 °C. On the other hand, the abundance of radiolarian
tests indicates colder oxygenated and eutrophic upwelling
intervals. Occasional colonization of hemipelagic bottom by
infaunal trace maker assemblage indicates that the bottom
water layer was not stagnant but periodically affected by con-
tour intermediate and low velocity currents. Hüneke & Stow
(2008) characterized contourite beds by fine lamination and
remnants of micro-cross-lamination of silty particles, domi-
nance of skeletal fragments of planktonic organisms, paucity
of benthic shells, thorough bioturbation and burrowing of the
underlying layer, dominance of microfacies of packed biomi-
crites, including wackestones and (foraminiferal) packstones,
calcilutites with calcisiltite lenses, and so similar to the
situation observed in the Strapkova section. The contourites
should have been deposited on the foot of continental slope
at a depth of more than 300 metres. Enhanced water dynamics
could be responsible for microfossil redeposition and for
several apparent blooms of crassicollarians. Temperature,
salinity changes and raised trace metal contents in sea water
could result in thinning and deformation of crassicollarian
loricas (Tappan 1993; Reháková 2000b; Vandenbroucke et
al. 2015) observed in several beds (296.3–297 m).

Sedimentation rate

The overall sedimentation rate increases up section, from

7.7 m/Myr in magnetozone M19r, through 9.5–9.8 m/Myr in
M19n and M18r to 12.7 m/Myr in M18n and at least

15 m/Myr in M17r (see Table 2). This trend is in agreement
with the data of Grabowski & Pszcz kowski (2006), who
also documented an increasing sedimentation rate between
the magnetozones M19r and M17r in the Po rednie section
(Fig. 18). Sedimentation rate in the Strapkova section is
gene rally higher than in the Po rednie section although the

shape of curves does not exactly coincide (Fig. 18). It is also
much higher than in the Brodno section, where it does not
exceed 3 m/Myr in the M19r and M19n magnetozones
(Houša et al. 1999). Compared with the South Alpine sec-
tions, the sedimentation rate in the Strapkova section is com-
parable to that in the Torre de Busi section in the Lombardian
Basin (Channell et al. 2010; Grabowski 2011). It is higher
than the sedimentation rate calculated for Trento Plateau sec-
tions (mostly 2–6 m/Myr in the M19r–M18n interval). It could
indicate a more distal depositional setting of the Strapkova
section in comparison with the Brodno section (Fig. 18).

Magnetic susceptibility and stratigraphic correlations

Magnetic susceptibility in pelagic and hemipelagic car-

bonates of Late Tithonian–Berriasian age is usually confined
to lithogenic influx into a basin (Grabowski et al. 2013;
2014). This is most probably also the case in the Strapkova
section, although geochemical data (e.g., correlation between
lithogenic elements and MS) are not available. The MS curve
obtained in the Strapkova section might be well correlated
with coeval intervals in the Brodno section (Houša et al.
1999) and in the Po rednie III section from the Tatra Mts.
(Grabowski et al. 2013). A long term decreasing MS trend
between the Upper Tithonian and upper part of the Lower
Berriasian (i.e. top of M20n and M17r) is well constrained in
the Po rednie and Strapkova sections (Fig. 19). A part of this
trend is also observed in the Brodno section between

M19r and M18r. Short-term MS fluctuations might be
compared as well.

Fig. 18. Sedimentation rates in the Strapkova section compared with
the Brodno section (PKB) and Po rednie section (Tatra Mts., Fatric
succession).

Magnetozone

Interval

(m)

Thickness

(m)

Duration

(My)

Sedimentation

rate (m/My)

M17r

48.4–26.75

21.65

1.44 (142.57–144.0)

15.0 (at least)

M18n

26.75–18.75

0.63 (144.0–144.63)

12.7

M18r

18.75–15.25

3.5

0.37 (144.64–145.01)

9.5

M19n

15.25–2.75

12.5

1.27 (145.01–146.28)

9.8

M19r

2.75–0.75

0.26 (146.28–146.54)

7.7

Attempt of sedimentation rate estimation in the Strapkova

section (timescale after Ogg, 2012).

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A decreasing trend I occurs between the uppermost part of

M20n, through M19r to the lower part of M19n2n. It is fol-
lowed by a gently increasing trend II, which terminates in
the upper part of M19n2n in the Strapkova and Po rednie
sections and in the middle part of this magnetozone in the
Brodno section. Trend II in the Po rednie III and Brodno sec-
tions terminates exactly at the J/K boundary, but in the Strap-
kova section — in the lower part of the Alpina Subzone.

The next decreasing trend III falls in the uppermost part

of M19n2n, approximately up to the M19n1r (Brodno) mag-
netozone. Trend IV reveals a generally increasing character
and culminates in a local MS maximum in the magnetozone
M18n. It is well resolved in the Strapkova and Po rednie sec-
tions, while most probably only the lowermost part of this
trend is observed in the Brodno section.

Trend V is related to profound MS decrease in the upper

part of M18n and in M17r, covering the uppermost part of the
Alpina Subzone, through the entire Ferasini Subzone and
a large part of the Elliptica Subzone. Trends I–V are
apparently synchronous in relation to magnetostratigraphy.
They might reflect changes of detrital input to the Pieniny
and Zliechov (Central West Carpathians) basins controlled
by regional tectonics and/or climate (Michalík 2007). The
third, eustatic component (Grabowski et al. 2013), can be

Fig. 19. Integrated correlation between Strapkova, Brodno and Po rednie III sections based on bio-, magnetostratigraphy and magnetic
susceptibility. Position of the Jurassic/Cretaceous boundary is indicated according to different de nitions: black arrow - Intermedia/Alpina
subzonal boundary; gray arrow - Colomi/Alpina subzonal boundary. Trends in MS variations (Roman numerals) are explained in the text.

involved after thorough correlation of well-dated but
geographically remote sections.

MS variations in the Strapkova section negatively correlate

with CaCO

content (see Fig. 16). The CaCO

increase

between beds 292 and 333 matches well the MS decrease
(trends I to III and the lower part of trend IV). The upper part
of trend IV (with maximum MS values in lower part of
M18n) might be compared with a slight decrease of CaCO

(beds 334 to 337). The final decrease of MS during trend
V correlates exactly with increasing CaCO

in the uppermost

Alpina, Ferasini and Elliptica subzones. Comparison of MS
trends with nannofossil data (Fig. 16) indicates climatic
control of MS variations. The abundance of Conusphaera
(relative cooling) coincides with the high MS values of
trends I to IV. The Nannoconus dominance (relative warming)
is related to decreasing MS trend (trend V). Notably, the MS
also correlates with sequence stratigraphy. Sequence boun-
daries and total plankton abundance maxima match with
local MS highs (see Figs. 5a and 16).

There is an apparent contradiction between magnetic stra-

tigraphy and biostratigraphy especially in the detailed situa-
tion of the JKB. It might be related to the fact, that the JKB
was defined according to slightly different criteria. In the
Po rednie III (Grabowski & Pszcz kowski 2006) and

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Brodno sections (Houša et al. 1999), the boundary was defined
as the Intermedia/Alpina subzonal boundary. Alternatively, the
Colomi/Alpina subzonal boundary was selected as the JKB
marker in a revised version of the Brodno (Michalík et al.
2009) and in the Strapkova (this study) biostratigraphy. The
Colomi/Alpina subzonal boundary is correlated with the top-
most part of M19n2n (Michalík et al. 2009) in the Brodno sec-
tion, but in the Strapkova section with its lower half. Accor-
ding to defined MS trends, the Colomi/Alpina boundary falls
at the boundary between trends III and IV in the Brodno sec-
tion and between trends I and II in the Strapkova (Fig. 19)
section. The Intermedia/Alpina subzonal boundary is

apparently synchronous in the Po rednie and Brodno
sections. It is situa ted in M19n2n, almost exactly between
trends II and III, close to the local MS maximum. However,
more high-resolution MS curves are desired, in order to test
if the MS trends observed are also present in other sections
beyond the Zliechov and the Pieniny basins.

The high-resolution analysis of calpionellid and dinofla-

gellate associations was used in order to characterize the JKB
interval in the Strapkova section. Three dinoflagellate and
four calpionellid zones have been recognized. They show
a Late Tithonian burst and calpionellid diversification and
a later decrease in diversity of crassicollarians. Such changes
in plankton composition and diversity across the Jurassic/
Cretaceous boundary were also documented by Reháková
(2000), Reháková in Michalík et al. (2009), Wimbledon et al.
(2013), Grabowski et al. (2010). The onset of the Alpina Sub-
zone of the standard Calpionella Zone, used as a marker for
the JKB, was documented in sample 298. This limit is defined
by morphological change of Calpionella alpina tests. There,
medium-sized spherical forms of Calpionella alpina domi-
nate in biomicrite limestone and are accompanied by calci-
fied radiolarians. The successive Ferasini Subzone characte-
rized by the FO of Remaniella ferasini was identified in
sample 340. In sample 344, Calpionella elliptica, the bio-
marker of the Elliptica Subzone appeared.

Nannofossil distribution documents the Tithonian NJT 17b

Subzone to Early Berriasian NKT and NK-1 nannofossil
zones (sensu Casellato 2010; and Bralower et al. 1989). The
first occurrence of Nannoconus wintereri, which indicates
the beginning of the NJT 17b Subzone and at the same time
the beginning of the JKB transition has been located in
sample 298.1.

Correlation of calcareous microplankton with C and O

stable isotopes and TOC/CaCO

data distribution was used in

characterization of the JKB interval.

C values ranging

from 1.1 to 1.4 ‰ (PDB) indicated a typical balanced regime
of carbon in the sea water. Negative

O shift from –1.5 to

–2.3 ‰ (V-PDB) in the uppermost Tithonian indicates a tem-
perature rise of 2–3° followed by stable temperature regime
during the JKB with a warming tendency higher up the

section. Radiolarian laminites interpreted as contourites and
bioturbation levels prove oxygenation events of bottom
waters during the Berriasian.

Primary magnetization of mixed polarity was isolated and

correlated with the Global Polarity Time Scale. The lower
part of the Crassicolaria Zone (up to the middle part of the
Intermedia Subzone) correlates with the M19r magnetozone.
The M19n magnetozone includes the upper part of the
Crassicollaria Zone and lower part of the Alpina Subzone.
The reversed Brodno magnetosubzone (M19n1r) was
identified in the uppermost part of M19n. The tops of the
M18r and M18n magnetozones are located in the upper part
of the Alpina Subzone and in the middle part of the Ferasini
Subzone, respectively. The Ferasini/Elliptica subzonal
boundary is located in the lowermost part of the M17r
magnetozone.

General MS decrease between the upper Tithonian and

Berriasian is in agreement with the increasing content of
CaCO

and warming trend documented by nannofossils. It is

also accompanied by an increasing sedimentation rate resul-
ting from higher carbonate productivity.

It appears that the MS might be of some importance in pre-

cise correlation of calpionellid bioevents. Minor MS varia-
tions in magnetozones M19r and M19n, related to changes of
detrital input, correlate between sections from the Pieniny
Klippen Belt (Strapkova and Brodno sections) and Tatra Mts
(Po rednie section). They clearly demonstrate a subtle dia-
chronism between Crassicollaria/Calpionella zonal boun-
daries, defined according to different criteria.

The authors thank T. Sztyrak,

K. í ková and K. Fekete for their help during eld work.
Dr. V. Šimo is acknowledged for determination and comments
on ichnofossils. The research was supported by the VEGA
Project 2/0034/16 and 2/0057/16, as well as by the APVV
project 14-0118, projects 7AMB14SK201, RV067985831,
and project No. GACR 16-09979S of Czech Grant Agency.
Palaeomagnetic and rock magnetic investi gations were nan-
cially supported by the project DEC-2011/03B/ST10/05256 of
the National Science Centre, Poland.

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Longicollaria dobeni (Borza, 1966)
Carpathella rumanica Pop, 1998
Borziella slovenica (Borza, 1969)
Dobeniella tithonica (Borza, 1969)
Chitinoidella boneti Doben, 1963
Dobeniella cubensis (Furrazola-Bermúdez, 1965)
Popiella oblongata Reháková, 2002
Praetintinnopsella andrusovi Borza, 1969
Crassicollaria intermedia (Durand Delga, 1957)
Crassicollaria massutiniana (Colom, 1948)
Crassicollaria brevis Remane, 1962
Crassicollaria parvula Remane, 1962
Crassicollaria colomi Doben, 1963
Calpionella alpina Lorenz, 1902
Calpionella grandalpina Nagy, 1986
Calpionella elliptalpina Nagy,1986
Calpionella elliptica Cadisch, 1932
Calpionella minuta Houša,1990
Tintinnopsella carpathica (Murgeanu and Filipescu, 1933)
Tintinopsella doliphormis (Colom, 1939)
Tintinnopsella longa (Colom, 1939)
Tintinnopsella remanei Borza1969
Remaniella ferasini (Catalano, 1965)
Remaniella catalanoi Pop, 1996
Remaniella duranddelgai Pop, 1996
Remaniella colomi Pop, 1996
Remaniella borzai Pop, 1996

Pop, 1996

Remaniella cadischiana Pop, 1996
Lorenziella hungarica Knauer and Nagy,1964

Stomiosphaera moluccana Wanner, 1940
Carpistomiosphaera borzai (Nagy, 1966)
Colomisphaera nagyi (Nagy, 1966)
Colomisphaera pulla (Borza, 1964)
Colomisphaera radiata (Vogler, 1941)
Colomisphaera tenuis (Nagy, 1966)
Colomisphaera fortis ehánek, 1992
Colomisphaera lapidosa (Colom, 1935)
Colomisphaera carpathica (Borza, 1964)
Parastomiosphaera malmica (Borza, 1964)
Stomiosphaerina proxima ehánek, 1987
Cadosina semiradiata fusca (Wanner,1940)
Cadosina semiradiata semiradiata (Wanner,1940)

Another microfossils
Gemeridella minuta Borza et Mišík 1975
Didemnoides moreti Durand-Delga
Didemnum carpaticum Borza et Mišík 1975
Globochaeta alpina Lombard 1945.

Assipetra infracretacea (Thierstein, 1973) Roth, 1973
Conusphaera mexicana (Trejo, 1969) subsp. mexicana Bralower in
Bralower et al. 1989
Conusphaera mexicana (Trejo, 1969) subsp. minor (Bown et
Cooper, 1989), Bralower in Bralower et al. 1989

(Manivit, 1966) Roth, 1973

Cyclagelosphaera margerelii Noël, 1965
Diazomatolithus lehmanii Noël, 1965
Faviconus multicolumnatus Bralower in Bralower et al. 1989
Hexalithus noeliae (Noël, 1956) Loeblich et Tappan, 1966
Lithraphidites carniolensis De andre, 1963
Microstaurus chiastius (Worsley, 1971) Bralower et al., 1989
Nannoconus sp. Kamptner, 1931
Nannoconus erbae Casellato, 2010
Nannoconus  globulus (Brönnimann, 1955) subsp. globulus
Bralower in Bralower et al. 1989
Nannoconus globulus (Brönnimann, 1955) subsp. minor Bralower
in Bralower et al. 1989
Nannoconus infans Bralower in Bralower et al. 1989
Nannoconus kamptneri (Brönnimann, 1955) subsp. minor Bralower
in Bralower et al. 1989
Nannoconus steinmannii (Kamptner, 1931) subsp. minor Deres et
Achéritéguy, 1980
Nannoconus  steinmannii (Kamptner, 1931) subsp. steinmannii
Deres et Achéritéguy, 1980
Nannoconus wintereri Bralower et Thierstein in Bralower et al. 1989
Polycostella beckmannii Thierstein, 1971
Retacapsa sp. Black, 1971
Watznaueria  barnesiae (Black in Black et Barnes, 1959) Perch-
Nielsen, 1968
Watznaueria biporta Bukry, 1969
Watznaueria britannica (Stradner, 1963) Reinhardt, 1964
Watznaureia fossacincta (Black, 1971a) Bown in Bown et Cooper
1989
Watznaueria manivitiae (Bukry, 1973) Moshkovitz et Ehrlich, 1987
Watznaueria ovata Bukry, 1969
Zeugrhabdotus embergeri (Noël, 1958) Perch-Nielsen, 1984
Zeugrhabdotus  erectus (Deflandre in Deflandre et Fert, 1954)
Reinhardt,  1965