Magneto- and biostratigraphy across the Jurassic-Cretaceous boundary in the Kurovice section, Western Carpathians, Czech Republic

Accepted Manuscript Magneto- and biostratigraphy across the Jurassic-Cretaceous boundary in the Kurovice section, Western Carpathians, Czech Republic T. Elbra, M. Bubík, D. Reháková, P. Schnabl, K. Čížková, P. Pruner, Š. Kdýr, A. Svobodová, L. Švábenická PII:

S0195-6671(17)30533-5

DOI:

10.1016/j.cretres.2018.03.016

Reference:

YCRES 3836

To appear in:

Cretaceous Research

Received Date: 8 December 2017 Revised Date:

16 March 2018

Accepted Date: 18 March 2018

Please cite this article as: Elbra, T., Bubík, M., Reháková, D., Schnabl, P., Čížková, K., Pruner, P., Kdýr, Š., Svobodová, A., Švábenická, L., Magneto- and biostratigraphy across the Jurassic-Cretaceous boundary in the Kurovice section, Western Carpathians, Czech Republic, Cretaceous Research (2018), doi: 10.1016/j.cretres.2018.03.016. This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.

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ACCEPTED MANUSCRIPT 1

Magneto- and biostratigraphy across the Jurassic-Cretaceous boundary in the Kurovice

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section, Western Carpathians, Czech Republic

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T. Elbraa, M. Bubíkb, D. Rehákovác, P. Schnabla, K. Čížkováa, P. Prunera, Š. Kdýra, A.

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Svobodováa, L. Švábenickád

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a

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Czech Republic ([email protected])

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b

Czech Geological Survey, Leitnerova 22, Brno 60200, Czech Republic

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c

Department of Geology and Palaeontology, Comenius University in Bratislava, Mlynská

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Institute of Geology of the Czech Academy of Sciences, Rozvojová 269, 165 00 Prague 6,

dolina, Ilkovičova 6, SK-842 15, Bratislava, Slovak Republic

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Czech Geological Survey, Klárov 131/3, 118 21 Prague, Czech Republic

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An integrated magneto- and biostratigraphic study of the Jurassic-Cretaceous (J-K) boundary

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section at Kurovice, Czech Republic was carried out. The acquired paleomagnetic data

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showed dual polarity characteristic remanent magnetization (ChRM) with counter-clockwise

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rotation direction. Rock magnetic data indicated magnetite as the principal carrier of

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remanent magnetization as well as presence of e.g. hematite and goethite. Magnetozones

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from M21n up to M17r were identified and dated as early Tithonian (dinoflagellate

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Semiradiata and nannofossil NJT15b zones) to late early Berriasian (Calpionella Elliptica

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and nannofossil NK-1 (sub)zones).

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Keywords: Jurassic-Cretaceous boundary, magnetostratigraphy, biostratigraphy, rock

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magnetism, calcareous micro- and nannofossils, Outer Flysch Carpathians

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ACCEPTED MANUSCRIPT 1. Introduction

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Integrating the magneto- and biostratigraphic data is vital calibration and correlation tool

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across the Jurassic-Cretaceous (J-K) boundary. Due to distinct magnetozone pattern around

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the J-K interval, it offers a link between different sections (marine, non-marine), bioprovinces

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(Tethyan, Boreal), and biostratigraphical (ammonite, calpionellid, etc.) scales as well as

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provides means to identify paleoenvironmental changes (e.g. Channell et al., 2010; Elbra et

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al., 2018 (in print); Grabowski and Pszczółkowski, 2006; Grabowski et al., 2010b; Houša et

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al., 2007; Michalík et al., 2009; Ogg et al., 1991; Pruner et al., 2010). Furthermore, the J-K

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boundary is fixed by the Berriasian Working Group using C. alpina in a magnetostratigraphic

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context (Ogg et al., 2016).

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In this paper, the first magnetostratigraphic data together with calpionellid, calcareous

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dinoflagellate and calcareous nannofossil stratigraphy of the Kurovice section in Outer

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Flysch Carpathians are presented.

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2. Geological setting

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The Kurovice section (49°16.4'N, 017°31.3'E; Fig. 1) is situated in an abandoned Kurovice

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quarry. It is located about 1.5 km south of Kurovice village and 2.6 km NE from Tlumačov.

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The Kurovice Limestone (Formation) occurs in the Outer Flysch Carpathians – a rootless

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allochthonous unit in the flange of the Carpathian Block with complex deformation history

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finished during the middle Miocene. The Outer Flysch Carpathians are built of uppermost

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Jurassic–lowermost Miocene deep-sea, predominantly turbidite, sediments deposited

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originally in the northern branch of Tethys Ocean. Deposition of the Kurovice Limestone is a

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response to Late Jurassic–Early Cretaceous rifting similarly to the Těšín (Cieszyn) Limestone

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of the Silesian Unit (e.g. Golonka et al., 2009). The Kurovice Limestone was deposited in the

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Magura Basin, more to the south of the Proto-Silesian Basin, and separated by the elevation

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ACCEPTED MANUSCRIPT of hypothetical Silesian Ridge (Golonka et al., 2014). After deformation and nappe transport

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several tectonic slices of the Kurovice Formation were placed to present positions along the

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main overthrust plane of the Magura Group of Nappes.

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The Kurovice Formation consists of micritic limestones, marlstones, silty marlstones,

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respectively wackestones, packstones and mudstones sensu Dunham (1962). Together with

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overlying Tlumačov Marlstone it composes a tectonic slice which is exposed on the surface

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in about 600 m long and up to 200 m wide area with bedding running in SW – NE direction.

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Sedimentary breccia (Upper Cretaceous) and sandstone flysch of the Soláň Formation (Upper

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Cretaceous–Paleocene) adjoin in the southeast (Rača Unit). In the northwest, the Rača Unit is

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thrusted over the clay-sandstone turbidites of the Ždánice-Hustopeče Formation (Oligocene–

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lowermost Miocene), which represent Krosno lithofacies of the Ždánice Unit.

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Kurovice Limestone was quarried since 1840 for local lime kiln and later Cement Factory in

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Tlumačov. The stratigraphy and geological position of the exposed and drilled limestones

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near Tlumačov were studied in 1960s (Benešová et al., 1968). The modern revision of

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stratigraphy was done by Eliáš et al. (1996) who assigned the Kurovice Limestone to the

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lower Tithonian–lower Berriasian and the Tlumačov Marlstones to the lower Berriasian–

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lower Valanginian.

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3. Sampling and methodology

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Bed by bed sampling of 148 limestone, marlstone and silty marlstone beds was carried out to

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study the stratigraphy of the Kurovice section.

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3.1

Magnetic properties

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Over 500 specimens were collected during several fieldwork campaigns for rock magnetic

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and paleomagnetic investigations. Magnetic susceptibility (κ) and its temperature dependence

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ACCEPTED MANUSCRIPT (χ-T), natural remanent magnetization (NRM), acquisition of isothermal remanent

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magnetization (IRM), Lowrie test (Lowrie, 1990) and paleomagnetic measurements: mainly

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thermal demagnetization (TD), occasionally also alternating field demagnetization (AF);

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were carried out at the Department of Paleomagnetism, Institute of Geology of the Czech

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Academy of Sciences.

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The stepwise thermal (up to 560-600 °C, in 40 °C intervals) and alternating field (up to 100-

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120 mT, in 3-10 mT intervals) demagnetization was performed to distinguish the remanent

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components. After each demagnetizing step, the intensity and direction of remanence were

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measured using a 2G Superconducting Rock Magnetometer 755 (2G SRM). For thermal

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demagnetization a Magnetic Measurements Thermal Demagnetizer MMTD80A and a

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MAVACS (Magnetic Vacuum Control System) apparatus were used. Additionally, the

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magnetic susceptibility was checked after each TD step using an AGICO KLF-4 Magnetic

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Susceptibility Meter. Resulting data was analysed with Remasoft software (Chadima and

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Hrouda, 2006).

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In order to determine the magnetic fabric, the temperature dependence of magnetic

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susceptibility of selected samples was measured (-192 °C to 700 °C, in an argon atmosphere)

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using an AGICO MFK1 kappabridge and the Curie temperatures (TC) were extracted.

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Isothermal remanent magnetization at increasing field strengths (up to 2 T) was induced

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using a MMPM10 pulse magnetizer and the acquired remanence was measured using AGICO

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JR-5 and JR-6A Spinner Magnetometers. Few samples were also subjected to 3-axes Lowrie

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(1990) test by magnetizing the samples in three perpendicular directions (x: 2 T, y: 300 mT,

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z: 100 mT; with MMPM 10) and then thermally demagnetizing as described before.

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3.2

Microfossils and microfacies

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ACCEPTED MANUSCRIPT The sampling for microfacies analyses and for documentation of succession of

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stratigraphically important calcareous microfossils – calpionellids and calcareous

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dinoflagellates, was carried out in 2016. Thin sections were prepared and studied under the

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LEICA DM 2500 transmitting light microscope in the Department of Geology and

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Palaeontology, Comenius University in Bratislava. Selected bioclasts and allochems

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(calpionellids, radiolarians, globochaetes, saccocomids, filaments, fragments of benthic

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organisms, quartz and lithoclasts) were identified. Microfacies and biomarkers were

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documented using an Axiocam ERc 5s camera. Dunham’s (1962) classification of

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microfacies was applied for the studied samples.

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3.3

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Nannofossils were analysed in smear slides in the fraction of 1-30 µm separated by

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decantation method using 7% solution of H2O2 (e.g. Švábenická, 2012). Slides were

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inspected under the Olympus BX51 and Nikon Microphot-FXA transmitting light

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microscopes using immersion objectives of ×100 magnifications. Nannofossil zones NJT,

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NKT and NK-1 were interpreted according to Casellato (2010) and Bralower et al. (1989).

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4. Results

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4.1

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Rock magnetic measurements divide samples into two groups (Fig. 2 left and right for group

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1 and 2, respectively). The coercivity spectra in acquisition curves (Fig. 2a and b) indicate

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two distinct magnetic fractions: of low and high coercivity, for all the samples throughout the

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Kurovice section. The low coercivity fraction (LC) reaches its saturation around 100-200 mT

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which is typical for magnetite. While samples in group 1 gain only ~50% of maximum

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magnetization by 100 mT and show no saturation by 2 T for high coercive fraction (HC), the

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ACCEPTED MANUSCRIPT group 2 indicates that saturation is either reached at ~1-2 T or is close to saturation and 75-

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95% of magnetization is gained by 100 mT. Saturation magnetization above 1 T could

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correspond to either hematite or oxyhydroxides such as goethite. Samples of group 1 are also

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more resistant to AF-demagnetization.

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The temperature dependent magnetic susceptibility (χ-T-curves) shows the presence of

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magnetite (TC~590 °C) as well as traces of hematite (TC>640 °C) and occasional goethite-like

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phase (TC~120-150 °C) for the samples in group 1 (Fig. 2c). Additionally, a possible

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occurrence of magnetic fraction with transition between 350-450 °C can be seen. Group 2

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(Fig. 2d) displays a very weak χ-T signal. Extracted Curie temperatures indicate the presence

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of mainly magnetite (possibly low concentration and with no distinct Hopkinson peak). Due

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to the weak nature of these samples, a presence of other magnetic minerals was hard to

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detect. The χ-T cooling curves show irreversible behaviour with production of new minerals

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below 590 °C (<660 °C for group 1; maximum peak ~360-450 °C) for all samples. In few

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samples a low temperature transition is observed ~-40 °C which could indicate slightly

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shifted and supressed Morin transition of hematite.

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Lowrie test (Fig. 2e and f) affirms the results of aforementioned methods. In all samples, (at

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T<400 °C) most of magnetization is carried by LC fraction with unblocking temperature

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(TUB) 560 °C (magnetite). In group 1, the HC fraction contributes to total magnetization

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below 400 °C and dominates the magnetic properties above 400-500 °C indicating the

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presence of hematite (TUB 640-680 °C). Several samples showed also a presence of goethite

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(represented by drop in HC magnetization around 120 °C; Supplement 1). In group 2, the

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magnetite controls the magnetization also above 400 °C while HC minerals are mostly absent

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or do not contribute much toward total magnetization. The Lowrie test demonstrates also the

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presence of minor amounts of medium coercive fraction (MC; unblocking temperature ~320-

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480 °C) throughout the section.

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ACCEPTED MANUSCRIPT The multicomponent analysis (after Kirschvink, 1980) of paleomagnetic TD demagnetization

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data (Fig. 3) reveals the presence of several magnetic components (Table 1): low temperature

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A-component (<~200 °C) which is close to the present Earth geomagnetic field for Kurovice;

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medium temperature reversed polarity remagnetization component (B; ~310 °C); and

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medium-to-high temperature (above 400 °C; occasionally up to 560 °C) C-component. The

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C-component was identified as ChRM (characteristic remanence) component. The ChRM

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holds dual polarity (Fig. 4). The mean direction, after tectonic correction, for normal polarity

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(labelled as CN) component is D = 208.2°, I = 39.2°, α95 = 4.2°, and for reverse polarity (CR-

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component) D = 18.7°, I = -50.3°, α95 = 6.9°. The upper Tithonian and lower Berriasian

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ChRM components are same within the α95 confidence level. Even though there are not

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enough samples with reversed ChRM for sufficient evaluation, the directions of CN and CR

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components seem to be antipodal with 167° angle between the Fisher means, which could

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correspond to classification C (McFadden and McElhinny, 1990).

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Intensity of remanent magnetization reveals that 50% of magnetization is, in most cases,

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removed ~100 °C. In many samples, the magnetization re-increased after demagnetization of

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A-component and dropped again below 50% between 200-400 °C, in few cases >400 °C.

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Several TD specimens showed too low or unstable remanent magnetization to be interpreted

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correctly and were discarded. Many samples showed also the changes in mineral phase –

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displayed by the rise of magnetic susceptibility; around 500 °C (occasionally already around

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400 °C). The unblocking temperatures, in conjunction with results of rock magnetic

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experiments, indicate that goethite and magnetite are most probable carriers of A and ChRM

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components, respectively. The carrier for remagnetized B component is uncertain as ~310 °C

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could correspond to several minerals, such as sulphides, maghemites or titano-magnetites.

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ACCEPTED MANUSCRIPT The AF demagnetization shows that samples are of either low or high coercivity. However,

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all the AF demagnetization data (Fig. 3) was disregarded due to potential content of

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secondary goethite.

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The value of the virtual geomagnetic pole (VGP) was calculated for tilt corrected ChRM

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(Table 2). This primary Tithonian/Berriasian direction of Kurovice section implies an

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extremely large counter-clockwise rotation, and obtained paleolatitude of ca. 24°N is in good

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agreement with data given by other authors for nearby localities (e.g. Brodno 27°N, Houša et

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al., 1996; Strapkova 24°N, Michalík et al., 2016; Western Tatra Mts. 28°N, Grabowski,

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2005).

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4.2

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Acquisition of paleomagnetic data across the J-K boundary strata allowed the construction of

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magnetostratigraphic profile. Six normal (N1-N6) and six reverse (R1-R6) polarity zones

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were identified (Fig. 5). The first magnetozone (R1) encompasses approximately 5 m interval

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at the top of Kurovice section. The component shows clearly the reversed polarity, which was

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occasionally counted using the Fisher mean, and the maximum angular deviation (MAD; or

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α95 for samples where ChRM was calculated using Fisher (1953) statistics) varies from 4° to

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25°. Two specimens at the top and one in the middle part of the interval show positive

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inclination; however, the declination of these specimens does not match the normal polarity

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ChRM direction, and hence were disregarded. The NRM of this interval is in average

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0.13 mA/m, with exception of one specimen with NRM 0.87 mA/m, and the average

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susceptibility of 16 E-6 SI. The next magnetozone (N1) holds normal polarity and has average

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MAD angle ~9°. NRM varies from 0.02 to 0.18 mA/m and κ from -6 to 26 E-6 SI, with higher

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magnetization values in the middle of the interval (κ shows opposite trend). Following

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reversed polarity zone (R2) is based on ChRM direction of 4 specimens, from which 1 mean

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Magnetic polarity zones

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ACCEPTED MANUSCRIPT direction was calculated by the Fisher mean (MAD = 7° and α95 = 34°, respectively). Besides

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above mentioned specimens, 2 additional specimens (1 with normal polarity and 1 without

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clear component) showed great circle trend towards reversed polarity and were included

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when determining the polarity zone. The average values of magnetization and susceptibility

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are 0.08 mA/m and ~19 E-6 SI, respectively. Next 2 magnetozones, N2 and R3, are based on

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only 3 normal (2 with clear C-component but MAD ~14° and 1 with positive inclination but

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‘incorrect’ declination) and 1 reversed polarity (MAD = 23°) data points, respectively. Exact

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boundary between them was hard to determine due to 1.5m sampling gap. The average NRM

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of N2 is 0.08 mA/m and κ = 11 E-6 SI with slight upward increase, and for R3: 0.1 mA/m and

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20 E-6 SI, respectively. Magnetozone N3 is approximately 19 m thick and consists of samples

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with relatively clear normal polarities. Fisher mean was used to determine direction in few

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specimens. Three samples were discarded from further evaluation: 2 showed negative

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inclination with declination similar to normal polarity samples (position of 1 of these 2

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samples coincides with location of slumping within the sample bed) and 1 positive inclination

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sample with northward declination. The MAD (α95) in the interval varies between 3° and 30°,

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NRM = 0.17 mA/m and κ = 15 E-6 SI. The following magnetozone R4 comprises of 2

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specimens with reversed polarity component (1 using Fisher mean; MAD and α95 14° and

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25°, respectively) and 2 specimens which indicated the reverse polarity trend in great circle.

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The average NRM is 0.07 mA/m and κ 20 E-6 SI. Magnetozone N4 starts with ‘well behaved’

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specimen, with relatively ‘high’ remanent magnetization (0.3 mA/m) but continues with

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magnetically

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NRM = 0.13 mA/m, κ = 20 E-6 SI). Fifth reversed polarity zone (R5) starts with sample with

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3 parallel specimens: 1 reversed (by Fisher mean), 1 with reversed trend in great circle and 1

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of normal polarity. This is followed by sample which again indicated the reversed trend in

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great circle, and 2 samples with Fisher mean normal and reversed polarities, respectively. The

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α95 of the 2 reversed polarity samples exceeds 30°. The succeeding normal polarity zone N5

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continues with short interval which seems to display intrinsic pattern of fluctuating

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declinations due to few specimens with unstable remanent component (disregarded). Lower

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part of this zone is relatively more stable, in few cases the Fisher mean was used to calculate

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the

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Magnetozone R6 (NRM = 0.1 mA/m, κ = 17 E-6 SI) consists of 1 specimen with reversed

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polarity (MAD = 8°), 1 with positive inclination but ‘erroneous’ declination, and 3 specimens

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which indicated trend towards reversed polarity in great circle. In the lowermost part of

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Kurovice section lays magnetozone N6 (MAD in upper part of the zone ~19° and in lower

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NRM = 0.11 mA/m,

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part ~7°; NRM = 0.13 mA/m and κ = 21 E-6 SI both display slight decrease upward).

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mean

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Calpionellid and calcareous dinocyst zonation

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Calpionellids are generally rare and hyaline forms dominate in the Kurovice section. In the

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Kurovice Limestone the calpionellids are relatively well-preserved. Microgranular

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chitinoidellids were not observed possibly due to dominance of microorganisms preferring

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silica. Standard calpionellid zones and subzones as proposed by Remane et al. (1986),

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Reháková and Michalík (1997) and the calcareous dinoflagellate succession by Reháková

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(2000) were used. The resulting biostratigraphy together with calpionellid and selected

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calcareous dinocyst distribution is presented in Fig. 5 and description of biozones is given

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below. A detailed description and complete list of cyst and calpionellid species, as well as

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nannofossils, will be published in Svobodová et al. (in preparation).

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Lower Tithonian Semiradiata Zone is positioned in the lower part of the Kurovice section

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(sample beds 1-35). Biomicrite, pelbiomicrite, pelbiointraclastic limestones and marly

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limestones to silty marlstones outline this zone. Rocks are slightly laminated and locally

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bioturbated or exhibit slightly recrystallized or silicified matrix and microfossils

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ACCEPTED MANUSCRIPT (wackestones, packstones and mudstones). Matrix is locally rich in pyrite and organic matter.

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Locally also a distinct gradation of allochems can be seen. Sediments obtain silty clastic

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admixture composed of quartz, muscovite and rare glauconite.

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Calcified radiolarians and sponge spicules determine prevailed type of the microfacies

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(spiculite-radiolarian, radiolarian-spiculite) generally in whole section. The zonal marker

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Cadosina semiradiata semiradiata is accompanied by abundant Cadosina semiradiata fusca.

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Upper Tithonian Tenuis-Fortis Zone (sample beds 36-42) follows the Semiradiata Zone. It

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was not possible to strictly separate the Tenuis and Fortis zones (Řehánek, 1992), resulting in

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one transitional zone. According to Reháková (2000) the Fortis Zone coincides with abrupt

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ecoevents in calpionellid associations: chitinoidellid disappeareance and their substitution

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with first transitional hyaline-microgranular calpionellids of the Praetintinnopsella Zone. The

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lorica of Praetintinnopsella andrusovi was identified just above in the sample 42/43 in the

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frame of the first Crassicollarian subzone what confirms above mentioned statement.

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Biomicrite, pelbiomicrite limestones of spiculite and radiolarian-spiculite microfacies

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(wackestones to packstones) are locally bioturbated or slightly laminated. Framboidal pyrite

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is scattered in matrix within few beds. The zonal markers Colomisphaera cf. tenuis and

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Colomisphaera fortis were documented among the cyst associations. Some cyst occurrences

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indicate redeposition from lower Tithonian sediments.

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Upper Tithonian Remanei Subzone, Crassicollaria Zone is situated between sample beds

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42/43 and 51/52. Succession of very rare calpionellids (Tintinnopsella remanei,

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Crassicollaria intermedia, Crassicollaria massutiniana, Crassicollaria parvula, Calpionella

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alpina) allowed establishing this first Crassicollarian subzone in biomicrite, pelbiomicrite

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limestones of spiculite and radiolarian-spiculite microfacies (wackestones, packstones to

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mudstones). Some beds contain pyrite.

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ACCEPTED MANUSCRIPT The character of sediments and microfacies in Crassicollaria Zone, Intermedia Subzone

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(sample beds 52-70) remains the same as was in the Remanei Subzone. The sample from bed

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66 shows the erosive surface and separates slightly laminated wackestone to mudstone

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biomicrite interval from graded pelbiomicrosparite grainstone in which clasts of volcanite

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rocks were observed. Above this bed the presence of more frutextites, in combination with

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radiolarians prevailed in microfacies, is observed. Calpionellids are more common. In their

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associations Crassicollaria parvula, Crassicollaria intermedia, Crassicollaria massutiniana,

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Crassicollaria brevis, Calpionella alpina, Calpionella elliptalpina, Calpionella grandalpina,

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Tintinnopsella carpathica were observed. There are still mixed cyst associations being

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influenced by enhanced water dynamics and resedimentation of older deposits. Some of

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crassicollarian loricas are deformed.

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Colomi Subzone, Crassicollaria Zone is exposed between sample beds 70/71 and 84.

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Biomicrite, pelbiomicrite, slightly laminated and locally bioturbated limestones of spiculite-

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radiolarian microfacies (wackestones, packstones, occasionally mudstones) are seen.

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Allochems are locally graded. Some of bioclasts and occasional matrix are silicified. Matrix

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is locally rich in scattered pyrite and organic matter (tiny plant fragments). Crassicollaria

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parvula, Crassicollaria massutiniana and Crassicollaria brevis prevail over Calpionella

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alpina and Tintinnopsella carpathica. Few species of Calpionella grandalpina and

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Calpionella elliptalpina were also identified. Abundance of cysts decreases in this zone.

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Lower Berriasian Calpionella Zone, Alpina Subzone (sensu Pop, 1974; Remane et al., 1986;

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Reháková and Michalík, 1997; Lakova et al., 1999; Boughdiri et al., 2006; Andreini et al.,

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2007; Lakova and Petrova, 2013) is located within sample beds 85/86 to 107(?) or 118.

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Biomicrite, slightly laminated and locally bioturbated limestones of spiculite-radiolarian

24

microfacies (wackestones to mudstones) are found. Further, the pelbiomicrite, microbreccia,

25

slightly laminated limestones bearing the bioclasts derived from carbonate ramp

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ACCEPTED MANUSCRIPT environment, extraclasts of dolomite limestones, Tithonian micrite crassicollarian limestones,

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clay shales and volcanic rocks were identified. The dominance of small spherical forms of

3

Calpionella alpina was the marker for the zone and subzone determination. Very rare

4

Crassicollaria parvula, Tintinnopsella carpathica, Calpionella sp., with seldom redeposited

5

Calpionella elliptalpina, Calpionella grandalpina and common deformed crassicollarian

6

loricae were observed.

7

Calpionella Zone, Ferasini Subzone (beds 119-131) consists of slightly laminated

8

biomicrite and locally bioturbated limestones (wackestone, packstone, less also mudstones).

9

One bed of silty marlstone was also sampled. Matrix contains scattered pyrite, silty admixture

10

and it is penetrated by calcite veins. Calcified radiolarians and sponge spicules determine the

11

microfacies prevailed in biomicrite limestones. Calpionellids decrease in abundance.

12

Remaniella duranddelgai was identified as the first remaniellid species. Thus, the first

13

appearance of index marker Remaniella ferasini is supposed to be situated few beds below.

14

Calpionellid association contains also Remaniella catalanoi, Remaniella colomi, Calpionella

15

alpina, Crassicollaria parvula, Tintinnopsella carpathica, Tintinnopsella doliphormis and

16

Lorenziella hungarica. Loricae of resedimented calpionellids have significantly thicker

17

calcite walls while loricae in autochnonous matrix are much thinner, bearing marks of

18

dissolution. Numerous deformed loricae occur.

19

Calpionella Zone, Elliptica Subzone (samples 132-148) is found in the topmost part of the

20

section. Biomicrite, slightly laminated, bioturbated or slightly recrystallized limestones of

21

spiculite-radiolarian microfacies (wackestones, mudstones and also packstones) and silty

22

slightly laminated limestones (mudstones) are found. Matrix contains scattered pyrite.

23

Calpionellids are very rare, many of them (mainly remaniellids) have their collars damaged

24

complicating the determination. The index marker Calpionella elliptica is accompanied by

25

Tintinnopsella carpathica, Lorenziella hungarica, Remaniella ferasini, Remaniella

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ACCEPTED MANUSCRIPT 1

duranddelgai, Remaniella colomi, Crassicollaria parvula and Calpionella alpina. Numerous

2

deformed loricas are documented. Cysts associations of all above mentioned Berriasian

3

calpionellid zones are mixed containing re-sedimented forms.

4 4.4

Calcareous nannofossil zonation

6

Calcareous nannofossils are usually poorly preserved. Assemblages are characterized by

7

dominance of Ellipsagelosphaeraceae, and by smaller numbers of stratigraphically significant

8

specimens of genera Conusphaera, Nannoconus and Polycostella. Other nannoliths and

9

placoliths are rare, fragmented and often cannot be identified (Svobodová et al., 2017,

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Švábenická et al., 2017).

11

Based on the presence of Polycostella beckmanii at base of sample 1, a nannoplankton Zone

12

NJT15b was recorded at the lower part of section within the cyst Semiradiata Zone (Fig. 5).

13

The overlying strata provided the first occurrences (FOs) of Helenea chiastia in the NJT16

14

Zone (sample 1 top) and Nannoconus globulus minor, which defines the base of NJT17a

15

Subzone (sample 55). The latter (NJT17a) occurs in the lower part of the calpionellid

16

Intermedia Subzone. Just above this bioevent, the last occurrence (LO) of Polycostella

17

beckmanii was captured. The FO of Nannoconus wintereri was found in the upper part of the

18

calpionellid Crassicollaria Zone (sample 79/80) and marks the base of the NJT17b Subzone.

19

The NJT17b continues up to the FO of Nannoconus steinmannii minor, NKT Zone (sample

20

92t). The base of NK-1 Zone, as indicated by FO of Nannoconus kamptneri kamptneri,

21

occurs in sample 124. In the overlying strata, yet other Berriasian nannofossils were found

22

like Speetonia colligata (sample 133/134) and Nannoconus steinmannii steinmannii (sample

23

140).

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5. Discussion

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ACCEPTED MANUSCRIPT Paleomagnetic data in conjunction with calpionellid, calcareous dinocyst and - nannofossil

2

zonation allowed to correlate the Kurovice section with the Global Polarity Time Scale

3

(GPTS; after Gradstein et al., 2012). The upmost magnetozone (R1) is identified as M17r.

4

This is in accordance with the data by Ogg et al. (1991), Grabowski and Pszczółkowski

5

(2006), Grabowski et al. (2010b) and Elbra et al. (2018; in print), where the base of the

6

Elliptica Subzone occurs within M17r magnetozone. The underlying normal magnetozone

7

N1 coincides with the Ferasini Subzone and is interpreted as M18n. The first occurrence

8

(FO) of Remaniella ferasini often falls within this magnetozone (e.g. Houša et al., 2004;

9

Pruner et al., 2010). Following this pattern, the R2 and N2 magnetozones, in the upper part of

10

Alpina and NKT (Sub)zones, should correspond to the M18r and M19n1n, respectively. Data

11

indicate that the Crassicollaria-Calpionella zonal boundary (base of the Alpina Subzone) lies

12

in the middle of our magnetozone N3 and, thus, must be unambiguously defined as

13

magneto(sub)zone M19n2n. The appearance of N. wintereri in this interval further proves the

14

interpretation of N3 as M19n2n. FO of N. wintereri in M19n2n has also been reported for e.g.

15

Torre de’Busi, St Bertrand and Puerto Escaño sections (Channell et al., 2010; Elbra et al.,

16

2018 (in print); Svobodová and Košťák, 2016). Furthermore, the range of NJT17b Subzone

17

points to the Tithonian-Berriasian boundary interval (Casellato, 2010). The last occurrence

18

(LO) of nannofossil P. beckmanii, species referred to be exclusively in the Tithonian

19

(Bralower et al., 1989), falls in the Kurovice section into the base of this magneto(sub)zone.

20

Between the N2 and N3 magnetozones appears 1 sample with reversed polarity. Based on the

21

identification of N2 and N3 as M19n1n and M19n2n, respectively, we believe that the

22

reversed polarity specimen could be a part of a narrow reversed polarity interval (R3)

23

corresponding to Brodno magneto(sub)zone (M19n1r). This interpretation is supported by

24

position of the suggested R3 magneto(sub)zone within the total thickness of magnetozone

25

M19n – at ~87%, which is similar to results from Brodno section (Houša et al., 1999) where

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ACCEPTED MANUSCRIPT the base of Brodno subzone was localized at the level of 82% in M19n. Further comparison

2

with European sections (Bosso: Houša et al., 2004; Strapkova: Michalík et al., 2016; Puerto

3

Escaño: Pruner et al., 2010) shows that Brodno subzone usually falls within 82-91% of the

4

total thickness of M19n. Due to sample disintegration during preparation, there appears about

5

1.5 m gap between reversed polarity specimen and normal polarity sample above it (within

6

the overlying M19n1n). Thus, the occurrence and exact boundaries of Brodno

7

magneto(sub)zone need to be further verified. Following reversed magnetozone R4 is situated

8

at the base of the Intermedia Subzone of Crassicollaria Standard Zone and is interpreted as

9

M19r similarly to several other Carpathian and Italian sites where M19r is situated entirely

10

within Intermedia Subzone (Grabowski and Pszczółkowski, 2006; Ogg et al., 1991). The top

11

of magnetozone M20n (M20n1n) falls within the Remanei Subzone. The narrow reversed

12

polarity interval (R5) was identified above the middle of the normal magnetozone M20n and

13

is interpreted as Kysuca magneto(sub)zone (M20n1r). The Kysuca magneto(sub)zone is often

14

detected, e.g. in Brodno (Michalík et al., 2009), Lókút (Grabowski et al., 2010a) and Puerto

15

Escaño section (Pruner et al., 2010), just above the base of the Remanei Subzone. In

16

Kurovice, the base of Crassicollaria Zone falls in the middle of Kysuca. The calcareous

17

dinoflagellates are used for biostratigraphic subdivision in the lower part of Kurovice section.

18

Following the magnetozone pattern, the dinoflagellate Tenuis-Fortis Zone is shown to

19

embrace the lower part of Kysuca magneto(sub)zone and upper part of M20n2n (N5).

20

Consequently, the lowermost reversed (R6) and normal (N6) polarity intervals, occurring in

21

the Semiradiata Zone, are interpreted as M20r and M21n, respectively. The identification of

22

N6 as magnetozone M21n is in accordance with the data of Michalík et al., (2009) and

23

Lukeneder et al., (2010), where the Semiradiata Zone extends to M21n.

24

Identification of the magnetozones enabled to estimate the approximate sedimentation rates

25

in the Kurovice section (Fig. 6). To compare the results to other Tethyan J-K sections all the

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ACCEPTED MANUSCRIPT sedimentation rates (after Channell et al., 1987; Channell et al., 2010; Elbra et al., 2018 (in

2

print); Grabowski and Pszczółkowski, 2006; Grabowski et al., 2010a; Houša et al., 2004;

3

Lukeneder et al., 2010; Michalík et al., 2009; Michalík et al., 2016; Ogg et al., 1991; Pruner

4

et al., 2010; Satolli et al., 2015) were (re-)calculated using the time-scales of Gradstein et al.

5

(2012). The values were estimated for whole magnetozones rather than for each subzone

6

separately and, thus, may differ from actual sedimentation rate for each separate subzone.

7

Sedimentation rates for top- and lowermost magnetozones represent, in most cases, the

8

minimum values, since these magnetozones are not complete.

9

Similarly to most other Tethyan sections, the overall sedimentation rate in Kurovice seems to

10

increase from the middle Tithonian to early Berriasian (Fig. 6). In several localities the

11

increase continues up to the middle of Berriasian. This increase is usually broadly attributed

12

to facies change and an increase of carbonate productivity as seen by bloom of calcareous

13

micro- and nannofossils (e.g. Grabowski and Pszczółkowski, 2006; Michalík et al., 2009;

14

Ogg et al., 1991). Grabowski et al. (2017) explained this raising trend as an increased

15

paleoproductivity related to aridization of the climate, decreased detrital input, and increased

16

upwelling in Carpathian part of Tethyan realm. The average Tithonian sedimentation rate in

17

Kurovice section is higher (M21n: ~8 m/Myr – M19n: 17 m/Myr) than recorded for other

18

Carpathian (localities 2-4 in Fig. 6) or Alpine Trento Plateau (7-11 in Fig. 6) sections. The

19

obtained values are closer to sedimentation rate of Torre de’Busi section in Lombardian

20

Basin during late Tithonian. Uppermost part of magnetozone M19 at Kurovice section (i.e.

21

bed 105) is characterized by few slump structures which originated in a short time interval.

22

Presence of these structures could partially explain the increased sedimentation rates. Slump

23

body containing rare clasts of volcanic and granitoid rocks, and occurrence of turbidites and

24

erosional channels suggest that the Kurovice Formation was deposited on the continental

25

slope. Pelagic sedimentation with large proportion of calcareous and siliceous marine

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ACCEPTED MANUSCRIPT microplankton prevailed, nevertheless, over the deposition from turbidite currents and

2

radiolarian-spiculite packstones. Most of "calcarenites" (fine to medium grained limestones)

3

are, according to thin-sections, radiolarian-spiculite packstones (Kiessling, 1996; Flügel,

4

2004). These packstones are not turbidites but more probably product of thermohaline bottom

5

currents (Stow et al., 2002). The velocity of currents did not allow sedimentation of micrite

6

fraction and affects the sedimentary rates. Possible decline of these currents might also

7

explain the increased sedimentation rates. The terrigenous clastic input can be neglected in

8

this time interval (M21n–M19n). The sedimentation rate in early Berriasian, displays in

9

Kurovice rapid decrease in magnetozone M18r. A slight decrease in sedimentation rate

10

during M18r is seen in many Tethyan sections, e.g. in Torre de’Busi, Strapkova and Frisoni

11

(Fig. 6). Sedimentation rate in M18n of Kurovice is similar to values reported for Western

12

Tatra Mts. (Fig. 6). Decreased rates in the upper part (M18r-M17r) of the Kurovice section

13

are probably caused by periods of non-deposition, as marked by hardgrounds and horizons

14

with Balanoglossites (complex burrowing-boring ichnostructure; Fig. 5). Moreover, hematite

15

is often associated with low sedimentation rate (Channell et al., 2000; Grabowski, 2011).

16

Rock magnetic studies of Kurovice samples indicate that even though magnetite is main

17

magnetic mineral throughout the section, the hematite (as seen in above described rock

18

magnetic group 1 samples) is occasionally seen. In Kurovice the presence of group 1 samples

19

(see Supplement 1) is found more often within, or close to, intervals with low sedimentation

20

rate, while among the high sedimentation rate intervals it’s found more seldom.

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6. Conclusions

23

Both the rock magnetic analyses and the values of unblocking temperatures point to

24

magnetite as the principal carrier of remanent magnetization. Additionally, a presence of

25

hematites, goethites and possible iron sulphides or maghemites was seen. Acquired

18

ACCEPTED MANUSCRIPT paleomagnetic data showed dual polarity ChRM. The direction of ChRM implies a counter-

2

clockwise rotation and ca. 24°N paleolatitude. Six normal and six reverse polarity zones were

3

identified and span from magnetozone M21n to M17r. Based on the calpionellids and

4

calcareous dinoflagellate succession the studied Kurovice Limestone Formation was dated as

5

early Tithonian (Semiradiata Zone), late Tithonian (Tenuis-Fortis Zone, Crassicollaria Zone)

6

to early Berriasian (Alpina, Ferasini and Elliptica Subzones of the Calpionella Zone). The

7

Kurovice section represents interval of nannofossil zones from NJT15b to NK-1. The

8

occurrence of Nannoconus wintereri highlights the M19n.2n magnetozone. Sedimentation

9

rate indicates general increasing trend from early Tithonian towards early Berriasian.

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We are thankful to two anonymous reviewers for their helpful reviews. This research is

13

supported by Czech Science Foundation [No. GA16-09979S]. The publication is in

14

concordance with research plan of the Institute of Geology of the Czech Academy of

15

Sciences [No. RVO67985831]. The research of Daniela Reháková was supported by the

16

VEGA Project [No. 2/0034/16 and 2/0057/16], as well as by the APVV project [No. 14

17

0118].

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Sobien, K., Schnabl, P., 2016. Stratigraphy, plankton communities, and magnetic proxies at

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the Jurassic/Cretaceous boundary in the Pieniny Klippen Belt (Western Carpathians,

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Slovakia). Cretaceous Research 67, 4, 303-328.

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Ogg, J.G., Hasenyager, R.W., Wimbledon, W.A., Channell, J.E.T., Bralower, T.J., 1991.

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Magnetostratigraphy of the Jurassic-Cretaceous boundary interval - Tethyan and English

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faunal realms. Cretaceous Research 12, 455-482.

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Ogg, J.G., Ogg, G.M., Gradstein, F.M., 2016. A Concise Geologic Time Scale 2016.

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Elsevier, Oxford, U.K.

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Pop, G., 1974. Les zones des Calpionelles Tithonique-Valanginiens du silon de Resita

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(Carpates meridionales). Revue Roumaine de Géologie Géophysique et Géographie, Série de

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géologie 18, 109-125.

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Pruner, P., Houša, V., Olóriz, F., Košták, M., Krs, M., Man, O., Schnabl, P., Venhodová, D.,

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Tavera, J.M., Mazuch, M., 2010. High-resolution magnetostratigraphy and biostratigraphic

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zonation of the Jurassic/Cretaceous boundary strata in the Puerto Escaño section (southern

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Spain). Cretaceous Research 31, 192-206.

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Reháková, D., 2000. Evolution and distribution of the Late Jurassic and Early Cretaceous

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calcareous dinoflagellates recorded in the Western Carpathians pelagic carbonate facies.

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Mineralia Slovaca 32, 79-88.

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ACCEPTED MANUSCRIPT Reháková, D., Michalík, J., 1997. Evolution and distribution of calpionellids – the most

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characteristic constituents of Lower Cretaceous Tethyan microplankton. Cretaceous Research

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18, 493-504.

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Řehánek, J., 1992. Valuable species of cadosinids and stomiosphaerids for determination of

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the Jurassic—Cretaceous boundary (vertical distribution, biozonation). Scripta 22, 117-122.

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Remane, J., Borza, K., Nagy, I., Bakalova-Ivanova, D., Knauer, J., Pop, G., Tardi-Filácz, E.,

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1986. Agreement on the subdivision of the standard calpionellid zones defined at the IInd

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Planktonic Conference Roma 1970. Acta Geologica Hungarica 29, 5-14.

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Satolli, S., Turtú, A., Donatelli, U., 2015. The terrigenous clastic input can be neglected in

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this time interval (M21n–M19n). Newsletters on Stratigraphy 48, 2, 153-177.

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Stow, D.A.V., Faugères, J.-C., Howe, J.A., Pudsey, C.J., Viana, A.R., 2002. Bottom currents,

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contourites and deep-sea sediment drifts: current state-of-the-art. In: Stow, D.A.V., Pudsey,

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C.J., Howe, J.A., Faugeres, J.-C., Viana, A.R. (Eds.): Deep-water contourite systems: Modern

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drifts and ancient series. Memoir. Geological Society of London, London, pp. 7-20.

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Švábenická, L., 2012. Nannofossil record across the Cenomanian–Coniacian interval in the

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Bohemian Cretaceous Basin and Tethyan foreland basins (Outer Western Carpathians),

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Czech Republic. Geologica Carpathica 63, 3, 201-217.

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Švábenická, L., Reháková, D., Svobodová, A., 2017. Calpionellid and nannofossil correlation

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across the Jurassic-Cretaceous boundary interval, Kurovice Quarry, Outer Western

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Carpathians. 10th International Symposium on the Cretaceous Vienna, August 21-26, 2017.

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Abstracts, p.252.

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Svobodová, A., Košťák, M., 2016. Calcareous nannofossils of the Jurassic/Cretaceous

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boundary strata in the Puerto Escaño section (southern Spain) – biostratigraphy and palaeo-

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ecology. Geologica Carpathica 67, 3, 223-238.

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ACCEPTED MANUSCRIPT Svobodová, A., Reháková, D., Švábenická, L., 2017. High resolution stratigraphy across the

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Jurassic-Cretaceous boundary in the Kurovice Quarry, Outer Western Carpathians, Czech

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Republic. Jurassica XIII, Abstracts and field trip quidebook, Poland, June 19-23, 2017, p.57.

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Svobodová, A., Švábenická, L., Reháková, D., Svobodová, M., Skupien, P., Elbra, T.,

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Schnabl, P., (in preparation). High resolution microbiostratigraphy across the Jurassic–

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Cretaceous boundary in the Kurovice section, Outer Western Carpathians, Czech Republic.

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Figure captions

2 Figure

1.

Geological

map

(left;

modified

after

Czech

Geological

Survey

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http://mapy.geology.cz/geocr_25/) and photo (right) of Kurovice section. Location of profile

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is marked with white line.

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Figure 2. Rock magnetic properties of the Kurovice limestone. Examples of group 1 and

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group 2 are displayed in left and right, respectively. a-b) Acquisition and demagnetization of

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isothermal remanence; c-d) Temperature dependence of magnetic susceptibility. Heating

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curves and running averages (grey lines) are displayed on top for better readability.

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Suggested transitions are pinpointed with arrows; and e-f) 3-axes Lowrie test – thermal

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demagnetization of isothermal remanent magnetization components in three perpendicular

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directions. M – Resultant intensity of total magnetization in 3 directions, k – magnetic

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susceptibility.

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Figure 3. Examples of thermal and alternating field demagnetization data: stereographic

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projection (left), Orthogonal (Zijderveld) vector projection (middle), and magnetization and

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susceptibility intensity curves (right). Grey arrows in Zijderveld plots of TD demagnetization

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illustrate the range and direction of the ChRM component.

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Figure 4. Stereographic projection of normal and reversed polarity C-component (closed and

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open symbols, respectively) of Jurassic and Cretaceous age in a) geographic (in situ)

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coordinates, b) after tilt correction, and c) in tilt coordinates after transferring the reversed

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polarities into normal and merging J-K data. The confidence intervals of average ChRM of

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components are displayed by dashed line.

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ACCEPTED MANUSCRIPT 1 Figure 5. Petrophysical and paleomagnetic data (left), and magneto- and biostratigraphy

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(right) of Kurovice section. GPTS is drawn according to Gradstein et al., (2012) and

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nannofossil zonation established after Cassellato (2010). Crosses in polarity column indicate

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the samples – with either normal polarity component or without any clear component; which

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indicated the great circle trend towards reversed polarity.

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Figure 6. Sedimentation rates in Kurovice (this work) and in other European J-K sections

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(after Channell et al., 1987: Xausa; Channell et al., 2010: Foza, Frisoni A, Colme di Vignola

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and Torre de’Busi; Elbra et al., 2018 (in print): St Bertrand; Grabowski and Pszczółkowski,

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2006: Western Tatra Mts.; Grabowski et al., 2010a: Lókút; Houša et al., 2004: Bosso;

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Lukender et al., 2010: Nutzhof; Michalík et al., 2009: Brodno; Michalík et al., 2016:

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Strapkova; Ogg et al., 1991: Mezzosilva; Pruner et al., 2010: Puerto Escaño; Satolli et al.,

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2015: Salto del Cieco). All sedimentation rates were (re)calculated for GPTS 2012 (Gradstein

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et al., 2012). Arrows display possible trends. The sedimentation rates of incomplete

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magnetozones display minimum values and are drawn using dashed boundaries.

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Tables.

2 Table 1. Mean directions of the remanence components.

CN CR CN+R

N R N*

In-situ directions Structural tilt correction Mean directions Mean directions Decl Incl Decl Incl α95 k α95 k [°] [°] [°] [°] lower Berriasian 239.7 32.4 6.6 14.2 198.6 44.2 5.5 20.3 66.6 -55.4 9.5 12.1 18.6 -52.7 8.2 16.3 241.6 40.6 6.0 10.9 198.6 47.2 4.6 18.2

CN CR CN+R

N R N*

251.0 63.2 250.6

upper Tithonian 5.5 9.7 212.4 13.1 28.6 19.1 5.24 10.1 211.7

36.5 -40.4 36.7

5.45 5.0 5.17

9.9 199.4 10.3

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32 18 50

67 4 71

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upper Tith. + lower Berr. A N 25.8 73.4 4.1 11.5 115.3 43.6 4.2 10.8 101 B R 174.9 -38.6 5.7 5.4 232 -57.9 5.3 6.1 113 N 247.3 32.5 4.3 10.6 208.2 39.2 4.2 11.2 99 CN CR R 65.7 -51.5 8.5 12.2 18.7 -50.3 6.9 18.6 22 CN+R N* 247.1 36.0 4.0 10.1 206.6 41.3 3.7 11.6 121 N – normal polarity, R – reverse polarity; * – reverse polarities were transferred into normal polarities; Decl – declination; Incl – inclination; α95 – 95% confidence limit; k – precision; n – number of samples; CN and CR components represent ChRM directions

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Table 2. Paleomagnetic data for the Kurovice locality. Mean Palaeomagnetic pole directions positions Age of rocks α95 k δp δm n Lat.λ Lon.φ Decl Incl Plat. Plon. Paleolat. [°]N [°]E [°] [°] [°]N [°]W [°]N l. Berriasian 198.6 47.2 4.6 18.2 10.6 179.0 28.4 4.1 6.3 50 49.27 17.55 211.7 36.7 5.17 10.3 14.8 13.0 u. Tithonian 20.5 3.8 6.4 71 u.Tith.+l.Berr. 206.6 41.3 3.7 11.6 13.2 7.4 23.7 2.9 4.8 121 Lat – latitude; Lon – longitude; Decl – declination; Incl – inclination; α95 – 95% confidence limit; k – precision; Plat – pole latitude; Plon – pole longitude; Paleolat – paleolatitude; δp and δm – confidence circles; n – number of samples

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ACCEPTED MANUSCRIPT Appendix 1

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List of calpionellids and calcareous dinoflagellates mentioned in the text in alphabetical order

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of genera.

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Cadosina semiradiata fusca Wanner, 1940

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Cadosina semiradiata semiradiata Wanner, 1940

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Calpionella alpina Lorenz, 1902

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Calpionella elliptalpina Nagy, 1986

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Calpionella elliptica Cadisch, 1932

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Calpionella grandalpina Nagy, 1986

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Colomisphaera fortis Řehánek, 1982

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Colomisphaera cf. tenuis Nagy, 1966

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Crassicollaria brevis Remane, 1962

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Crassicollaria intermedia Durand-Delga, 1957

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Crassicollaria massutiniana Colom, 1948

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Crassicollaria parvula Remane, 1962

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Lorenziella hungarica Knauer and Nagy, 1964

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Praetintinnopsella andrusovi Borza, 1969

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Remaniella catalanoi Pop, 1996

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Remaniella colomi Pop, 1996

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Remaniella duranddelgai Pop, 1996

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Remaniella ferasini Catalano, 1965

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Tintinnopsella carpathica Murgeanu and Filipescu, 1933

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Tintinnopsella doliphormis Colom, 1939

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Tintinnopsella remanei Borza, 1969

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ACCEPTED MANUSCRIPT List of calcareous nannofossils mentioned in the text in alphabetical order of genera.

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Helenea chiastia Worsley, 1971

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Nannoconus glubulus minor Bralower in Bralower et al. 1989

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Nannoconus kamptneri kamptneri Brönnimann, 1955

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Nannoconus steinmannii minor Deres and Achéritéguy, 1980

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Nannoconus steinmannii steinmannii Kamptner, 1931

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Nannoconus wintereri Bralower and Thierstein in Bralower et al. 1989

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Polycostella beckmanii Thierstein, 1971

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Speetonia colligata Black, 1971

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Supporting files.

2 Supplement 1 (Figure). Tilting, sedimentation rate with placement of rock magnetic (RM)

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groups, and examples of Lowrie test.

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Supplement 2 (Excel table). Magnetic data of Kurovice samples.

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Highlights • First magnetostratigraphic record of the Kurovice Jurassic-Cretaceous boundary section in Czech Republic. • New calpionellid, calcareous dinoflagellate and nannofossil biostratigraphy. • Kurovice section represents early Tithonian to late early Berriasian interval. • The base of Alpina Subzone and FO of Nannoconus wintereri highlight the JurassicCretaceous boundary interval within M19n.2n magnetozone. • Sedimentation rate increases from early Tithonian towards early Berriasian.