GeolCarp_Vol68_No5_385

GEOLOGICA CARPATHICA

, OCTOBER 2017, 68, 5, 385–402

doi: 10.1515/geoca-2017-0026

www.geologicacarpathica.com

An Albian demise of the carbonate platform

in the Manín Unit (Western Carpathians, Slovakia)

KAMIL FEKETE

, JÁN SOTÁK

2, 3

, DANIELA BOOROVÁ

, OTÍLIA LINTNEROVÁ

JOZEF MICHALÍK

and JACEK GRABOWSKI

Earth Science Institute of the Slovak Academy of Sciences, Dúbravská cesta 9, 840 05 Bratislava, Slovakia;

kamil.fekete@savba.sk; geolmich@savba.sk

Earth Science Institute of the Slovak Academy of Sciences, Ďumbierska 1, 974 01 Banská Bystrica, Slovakia; sotak@savbb.sk

Department of Geography, Faculty of Education, KU Ružomberok, Hrabovská cesta 1, 034 01 Ružomberok, Slovakia

State Geological Institute of Dionýz Štúr, Mlynská dolina 1, 817 04, Bratislava, Slovakia; daniela.boorova@geology.sk

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

Polish Geological Institute — National Research Institute, Rakowiecka 4, 00-975 Warsaw, Poland; jgra@pgi.gov.pl

(Manuscript received November 29, 2016; accepted in revised form June 9, 2017)

Abstract:

The production of platform carbonates of the Manín Unit (Manín Straits, Central Western Carpathians)

belonging to the Podhorie and Manín formations and formed by remains of rudists and benthic foraminifers (Urgonian-type

carbonates), was previously assumed to terminate during the Aptian. First, we show that these deposits were primarily

formed on the upper slope (Podhorie Formation) and in a fore-reef environment (Manín Formation). Second, biostrati-

graphic data indicate that the shallow-water production persisted up to the Albian, just as it did in another succession of

the Manín Unit. The Podhorie Fm contains colomiellids (Colomiella recta, C. mexicana) and calcareous dinoflagellates

(Calcisphaerula innominata) that indicate the Albian age. It also contains planktonic foraminifers (Ticinella roberti,

Ticinella cf. primula, Ticinella cf. madecassiana, Ticinella cf. praeticinensis) of the Albian Ticinella primula Zone.

The Podhorie Formation passes upwards into peri-reefal facies of the Manín Fm where we designate the Malý Manín

Member on the basis of rudists shell fragments and redeposited orbitolinids. Microfacies associations share similarities

with the Urgonian-type microfacies from Mediterranean Tethys and allow us to restrict the growth and the demise of the

carbonate platform. δ

C and δ

O isotopes change over a broad range of both formations: δ

C is in the range +1.03 to

+4.20 ‰ V-PDB and δ

O is in the range −0.14 to −5.55 ‰ V-PDB. Although a close correlation between δ

C and δ

indicates diagenetic overprint, a long-term increase of δ

C can indicate a gradual increase in the aragonite production

and/or increasing effects of oceanic water masses in the course of the Albian, prior to the final platform drowning.

Carbonate platform evolution was connected with submarine slumps and debris flows leading to redeposition and

accumulation of carbonate lithoclasts and bioclastic debris on the slope. Our study confirms that the growth of carbonate

platforms in the Central Western Carpathians was stopped and the platform collapsed during the Albian, in contrast to the

westernmost Tethys. A hardground formed during the Late Albian is overlain by Albian – Cenomanian marls of the

Butkov Formation with calcisphaerulid limestones characterized by planktonic foraminifers of the Parathalmanninella

appenninica Zone and calcareous dinoflagellates of the Innominata Acme Zone.

Keywords: Lower Cretaceous, Urgonian, Manín Fm, Podhorie Fm, planktonic foraminifers, rudists, C isotopes.

Introduction

Cretaceous carbonate platforms contain important information

on biotic changes, depositional facies, diagenesis, climatic

events, eustatic sea level fluctuations and terrigenous sedi-

ment influx, and provide clues to platform growth and demise

during the Early Cretaceous Tethys (Simo et al. 1993). During

the Late Jurassic and Early Cretaceous, several shallow marine

carbonate platforms evolved on both sides of the Penninic

Oceanic and on the southern Tethyan margins. During the

Barre mian and Early Aptian, the northern Tethyan area was

covered by a shallow sea where carbonate “Urgonian”-type

sediments were deposited (Arnaud-Vanneau 1980; Arnaud et

al. 1995; Peybernès et al. 2000; Masse & Fenerci-Masse 2011,

2013; Clavel et al. 2013).

In the western Tethys, shallow-water Urgonian-like carbo-

nates, including inner- and outer carbonate platform sediments

and biotas (Masse et al. 1992), were deposited mainly during

the Barremian and Early Aptian (Bedoulian). Their drowning

occurred repeatedly at multiple steps and was connected to

climatic and oceanographic changes, replacement of photozoan

carbonate producers by heterozoan producers, and to oceanic

anoxic crises in deeper basins (Masse 1989 a,b; Föllmi 2008;

Erba et al. 2015). Analyses of Urgonian carbonate platforms

significantly contributed to the understanding of paleo geo-

graphical, paleoecological and paleoclimatic changes through out

the Early Cretaceous (Godett et al. 2006; Föllmi & Gainon

2008; Föllmi 2012; Föllmi & Godet 2013). Bio strati graphic,

sedimentological and chemostratigraphical methods, in parti-

cular distribution of P and isotopic composition of C and O are

used for characterization of nutrient support, C cycling and defi-

nition of paleoceanic proxies but also for anoxic conditions in

basins, which acquired a global character during Oceanic anoxic

events (OAEs, see Föllmi & Godet 2013; Huck et al. 2013).

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The Urgonian-type limestones have been identified in seve-

ral areas of the Western Carpathians (Mišík 1990; Michalík

1994). In the Outer Carpathians, they occur exclusively as

exotic pebbles in younger deposits. In the Central Carpathians,

they are preserved in the Tatric Zone, in the Manín Unit, and

in the peripheral units of the Krížna Nappe (Michalík 1994;

Michalík et al. 2012, 2013). Firstly, in these units, the input of

clasts in platform carbonates indicated that the platform

growth was still active during the Late Aptian–Albian, sug-

gesting that the carbonate factory production in the Western

Carpathians terminated later than in other Tethyan regions

(Boorová 1990; Mišík 1990; Michalík et al. 2012). Second,

Michalík (1994) and Michalík et al. (2012) showed that the

carbonate production probably persisted up to the Early Albian

in the Manín Unit at Butkov. It remains poorly known whether

this late timing of the carbonate demise also applies to other

successions in the Western Carpathians.

Our aim is to document biostratigraphy and facies develop-

ment of platform carbonates of the Manín Unit outcropping in

the Manín Straits, previously assigned to the Barremian–

Aptian–“Urgonian” sequence in the Western Carpathians

(Köhler 1980; Rakús 1984; Michalík & Vašíček 1984; Boorová

1991; Boorová & Salaj 1996) (Fig. 1). Integrating sedimento-

logical, biostratigraphic and chemostratigraphical research

data allowed us to better constrain the environmental develop-

ment of carbonate platform in the Central Western Carpathians.

Geological setting

The Western Carpathians represent a part of the extensive

Alpine–Carpathian mountain system with very complicated

geological structure, composed of imbricated crustal segments

covered by differentiated sedimentary sequences (Plašienka et

al. 1997; Plašienka & Soták 2015). The Manín Unit is situated

at the Central Western Carpathian nappe front on the left side

of the Middle Váh Valley (Fig. 1A). It is partially involved in

a collisional accretionary wedge (Michalík & Žítt 1988;

Michalík et al. 2013). The paleogeographical position of the

Manín Unit and its relations to the Tatric and the Fatric units

or to the Pieniny Klippen- and Peri-Klippen zone are not

resolved. The Lower Cretaceous sequence (consisting of

Valanginian to Barremian pelagic limestones, covered by

Urgonian-type limestones) of the Manín Unit is similar to

marginal Central Carpathian units, whereas the Upper

Cretaceous sequence is composed of shales unlike in the

Central Carpathians, where the sedimentation was broken by

strong space reduction due to Alpine folding and nappe forma-

tion (Michalík et al. 2012, 2013).

The Urgonian-like limestones in the Manín Unit are divided

into slope facies of the Podhorie Fm and platform facies of the

Manín Fm. The Podhorie Fm, defined in the Butkov Quarry by

Borza et al. (1987), begins with a 4–5 m thick breccia member

formed by markedly gradational strata rhythms. Clasts consist

Fig. 1. A — Geographical map of Slovakia showing the Pieniny Klippen Belt and the location of the study area. B — Simplified geological

map of the area showing studied section (modified from Mello 2005). C — Schematic section through the Middle Jurassic (blue) – Lower

Cretaceous (green) formations of the Manín Straits with the examined section.

Manín creek

road

Považská Teplá
village

Záskalie
village

0.3

0.6 km

Záskalie village

Považská Teplá village

Malý Manín Mt.

M282

M178

Bratislava

Košice

Dunaj
river

Váh
river

CZECH R.

POLAND

SLOVAKIA

HUNGARY

17°00´

18°00´

19°00´

20°00´

21°00´

22°00´

49°00´

48°00´

22°00´

49°00´

48°00´

17°00´

18°00´

19°00´

20°00´

21°00´

40 km

80 m

Legend

Faults

Studied section

Praznov Formation

Butkov Formation

Podhorie and Manín fms

Kališčo Formation

Czorsztyn Formation

Trlenská Formation

Brts Formation

Hardground surface

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AN ALBIAN DEMISE OF THE CARBONATE PLATFORM IN THE MANÍN UNIT (WESTERN CARPATHIANS)

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, 2017, 68, 5, 385–402

of bioclastic as well as of micritic limestones, cherts, rarely of

fragments of basic extrusive clasts and tuffs. The clasts are of

Barremian to Early Aptian age. The upper member is formed

by bedded bituminous organodetritic limestones with blackish

grey cherts. They change upwards into the massive pale

organo genic limestone sequence of the Manín Fm (in the

sense of Michalík & Soták 1990). They are of biomicritic-

microsparitic character with fine-grained biogenic debris, cri-

noid columnals, bivalve shells and large benthic foraminifers,

rare planktonic foraminifers and colomiellids. The sequence is

terminated by a hardground surface and covered with dark

grey spotted marls of the Butkov Fm (Kysela et al. 1982), with

glauconitic grains in the basal part, containing Upper Albian

foraminifers.

The Manín Straits, exposing a sequence of Jurassic–

Cretaceous beds of the Manín Unit (Fig. 1B, C) is situated in

the area of the Strážovské vrchy Mts., northeast of the

Považská Teplá village (49°8’23.80” N, 18°30’30.80” E).

The first observation from this site came from Štúr (1860), he

described dark grey limestones with cherts and light grey

limestone conglomerates as an equivalent of the Štramberk-

type limestones. Andrusov (1945) examined a sequence of

Mesozoic rocks within a geological research of the Pieniny

Klippen belt. The first detailed section in the Manín Straits

was produced by Mišík (1957). More detailed investigations

of later authors (e.g., Köhler 1980; Michalík & Vašíček 1984;

Rakús 1984; Boorová 1991; Boorová & Salaj 1996) brought

new findings considering lithostratigraphy, fossil assemblages

and competed with its interpretations within the Manín Unit.

Material and methods

The more than ninety-metre-thick sequence of the Podhorie-

and Manín formations (Urgonian facies s. l.) and the so called

“calcisphaerulid limestone” (Borza et al. 1983) was sampled

in the Manín Straits. The rock samples were taken at metre

intervals and have been analysed for microfacies, microfossils,

nanofossils, cathodoluminescence, stable C- and O-isotope

composition, total organic carbon, total carbon content and

magnetic susceptibility.

Sedimentological and paleontological investigations have

been supported by analyses of 92 thin-sections. Microfacies

and biostratigraphically important markers have been docu-

mented in thin sections under optical microscopes Zeiss Axio

Scope. a1, Zeiss-JENAPOL, using an Olympus Camedia

C5060 and Axiocam 105 colour cameras. Volumetric contri-

butions of five main microcomponents, including micrite,

sparite, lithic clasts, heterozoans (i.e., large benthic foramini-

fers, brachiopods, molluscs, including rudists, echinoderms),

and photozoans (calcareous algae, including algal micro-

borings) were quantified. The microfacies characteristics with

environmental attributions are adopted from microfacies types

(F0 to F11) distinguished for the Lower Cretaceous Urgonian

platforms in SE France by Arnaud-Vanneau (1980). Generic

attributions of foraminiferal taxa are based on the classi fications

of Longoria (1974, 1984), Robaszyński & Caron (1979, 1995),

Loeblich & Tappan (1988) and Premoli-Silva & Verga (2004).

The carbonate classification follows the scheme of Dunham

(1962) and Folk (1959, 1962). Current facies classifications

are based on recent carbonate sediments and generalized

models of carbonate platforms (e.g., Wilson 1975; Arnaud-

Vanneau 1980; Masse & Fenerci-Masse 2011).

The calcareous nanofossils were processed by the decan-

tation method adapted from Švábenická (2001), adjusted

according Bom et al. (2015). We collected and studied 30 sam-

ples from the Podhorie and Manín formations using a Zeiss

light microscope with 1500× magnification. Due to very poor

preservation, 11 samples were taken from underlying beds of

the section (interval M179–M189) in order to obtain calca-

reous nannofossils. Perch-Nielsen (1985), Bown & Young

(1997) and Bown (1998) were used for their classifications.

Cathodoluminiscence records were carried out by a Neuser

HC-2 microscope (hot cathode) at the Department of Geological

Sciences of the Masaryk University in Brno using a polished

thin section from sample No. M261, coated with carbon.

92 bulk rock samples from the M190–M 282 interval of the

section were selected for geochemical analyses. Contents of

total carbon (TC) and total inorganic carbon (TIC) were

detected in rock-powder samples on the C-MAT 5500

device of the Ströhlein firm. Total organic carbon (TOC

)

content was obtained as the difference between TC and TIC

(TOC = TC − TIC), and CaCO

contents recalculated from TIC

are plotted in the scheme.

Isotope ratios of oxygen and carbon were analysed in CO

after standard decay of rock samples in 100 % phosphoric

acid. Analyses of carbonate samples were generated on the

Mass Spectrometer MAT253 equipped with the Gasbench

device (Thermo Scientific Samples). These data are given in

standard del-notation (δ) in promile (‰) with respect to the

Vienna International Isotopic Standard (V-PDB) with 0.01 ‰

accuracy. Geochemical analyses were carried out in the

Laboratories of the Earth Science Institute of the Slovak

Academy of Sciences (Centre of excellence for integrated

research of the Earth’s geosphere) in Banská Bystrica.

Mass normalized magnetic susceptibility (MS) was mea-

sured with MFK-1 kappabridge (AGICO, Brno) in the

Paleomagnetic Laboratory of the Polish Geological Institute

— National Research Institute. Small cubic samples of ca.

8 cm

volume were prepared for magnetic analyses.

Lithology

The carbonate platform sequence in the Manín Straits starts

with upper slope facies of organodetrital limestones and passes

upwards into peri-reef facies, with lateral replacement of these

two to a considerable extent coeval parts of one area of sedi-

mentation (carbonate platform and its slope). The thickness of

these Urgonian-like facies attains around 100 m.

Their basal part (up to 45 m) is represented by mainly grey

to darker grey, thick bedded to massive limestones with cherts

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, 2017, 68, 5, 385–402

in lower parts of the section (M178–M183) (Fig. 2). Based on

their position in the sequence (emerging in the basement of the

Manín Fm) and lithological character, we assign them to the

upper part of the Podhorie Fm although they do not completely

coincide with the original definition of the formation allocated

in the Butkov Quarry. Three major faults (Fig. 2) cut through

the limestones with no influence on the sequence succession.

The Podhorie Fm passes upwards continuously into the light

grey, massive, strongly recrystallized limestones of the Manín

Fm (around 55 m thick). The formation contains rudist shell

fragments typical for the section studied. The Manín Fm is

terminated by a hardground surface, which is covered by

marls and marlstones of the Butkov Fm. A thin layer of calci-

sphaerulid limestone occurs in the basal part of the Butkov Fm.

wackestone/

packstone

(biomicrite

biomicrosparite)

MFT

-1

Pseudothalmanninella

ticinensis

Zone

Innominata

Acme

Zone

MMM

rudist

reef

245

280

275

270

265

260

255

250

240

235

230

225

220

215

210

205

200

195

190

grainstone

(biomicrosparite)

MFT

-3

packstone

grainstone

(biomicrite

biomicrosparite)

MFT

-2

Butkov

185

180

Radiolarians

Marls and marlstones

Massive coarse-grained limestones

Bedded fine-grained limestones

Crumbling limestones

Rudists

Gastropods

Orbitolinas

Bivalves

Echinoids

Memorial

Presence of micrite

Presence of photozoans

Hard-ground surface

Calcisphaerulid limestones

Sponge spicules

Cherts

Sparite (%)

Micrite (%)

Heterozoans (%)

Lithic clasts (%)

grainstone/

rudstone

(biosparite

biosparrudite)

MFT

-4

grainstone/

rudstone

(biosparite

biosparrudite)

MFT

-4

M
M

icinella

Zone

Fig. 2. A scheme of stratigraphic division of the Manín and the Podhorie fms in the Manín Straits section. Left: chronostratigraphic division,

lithostratigraphy and microfacies following the scheme of Folk (1959, 1962). Right: Curves showing representation of constituents of the

Podhorie- and Manín formations.

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Microfacies and microfossils

We have identified four dominant facies types within the

Manín and Podhorie fms (Urgonian facies s. l.) in the Manín

Straits section, each of them pointing to a specific depositional

environment (Figs. 2, 3). They are represented by bioclastic

and peloidal wackestones and packestones (MFT-1), packstones

and grainstones (MFT-2), bioclastic grainstones (MFT-3), and

bioclastic grainstones and rudstones (MFT-4) (Fig. 2).

MFT-1: Wackestones and packstones

(biomicritite / biomicrosparite)

They form the basal part of the section represented by the

Podhorie Fm (interval M178–M203). This hemipelagic facies

deposited in circalittoral environments was formed under calm

conditions with weak currents (Arnaud-Vanneau 1980).

A spiculite-radiolarian microfacies in the lower horizons

(interval M178–M181) represents a more distal environment

with fine-grained debris of echinoderms,

sponge spicules of

various morphotypes, rare thin- and thick walled filaments,

radiolarians of the Spumellaria type, Ostracoda div. sp. and

fragments of echinoid spines. Upwards, they completely

disappear and sedimentary environment becomes shallower.

The matrix is composed of micrite, replaced by secondary

sparite in some places (Fig. 2). The proportion of micrite

matrix in lower horizons (interval M178–M185) is basically

the same as at the type locality of this formation at the Butkov

Quarry, with a slight decrease (10–15 %) upwards (Fig. 2).

Reef-building organisms derived from the carbonate platform

do not occur in the limestones.

Planktonic foraminifers are represented by high arched

globular chambered trochospiral forms. Some specimens can

be determined as Ticinella roberti (Gandolfi) (Fig. 4 A–C),

Ticinella cf. primula Luterbacher (Fig. 4 E–F), Ticinella cf.

madecassiana (Sigal) (Fig. 4 G–H), Ticinella cf. praetici nensis

(Sigal) (Fig. 4 D) of the Ticinella primula Zone (Premoli-Silva

& Verga 2004) mark the Middle Albian interval (Figs. 2, 3).

Rare colomiellids Colomiella mexicana Bonet (Fig. 4 L),

Colomiella recta Bonet (Fig. 4 M), Colomiella sp. and

calca reous dinoflagelates Calcisphaerula innominata Bonet

(Fig. 4 N), Colomisphaera gigantea (Borza) (Fig. 4 O), and

Cadosina semiradiata olzae (Nowak) also occur. Benthic for-

aminifers are represented by Bolivinopsis aff. capitata

Yakovlev (Fig. 5 A), Glomospirella gaultina Berthelin (Fig. 5 B),

Turri glomina? anatolica Altiner, Peybernès & Rey, 1968

(Fig. 5 C), Meandrospira favrei (Charollais, Bronnimann &

Zaninetti) (Fig. 5 D), Akcaya minuta Hofker (Fig. 5 E),

Dentalina sp. (Fig. 5 F), Haplophragmoides aff. vocontianus

Moullade (Fig. 5 G), Spirillina sp. (Fig. 5 H), Anomalina sp.,

Frondicularia sp., Patellina sp., Lenticulina sp., Gaudryina

sp. and Meandro spira sp. Redeposited calpionellids,

Crassicollaria parvula Remane, Calpionela alpina Lorenz,

Lorenziella hungarica Knauer & Nagy are present. Calcareous

nannofosils are rather rare and their preservation ranges from

moderate (only in a few samples) to extremely poor. We found

calcareous nannoplakton in samples No. M179, M180, M182,

M192 and M194. It is represented by Watznaueria barnesiae

(Black in Black & Barnes, 1959) Perch-Nielsen (Fig. 6 A–D),

Watznaueria biporta Bukry, 1969 (Fig. 6 E–F), Watznaueria

cynthae Worsley, 1971 (Fig. 6 I–J), Cyclagelosphaera sp.

(Fig. 6 K), Cretar habdus sp. (Fig. 6 L) and by reworked

Micrantholithus obtusus Stradner, 1963 (Fig. 6 G) and

Nannoconus bucheri Brönni mann, 1955 (Fig. 6 H). The last

stratigraphic occurrences of Micrantho lithus obtusus and

Nannoconus bucheri occur in the Late Aptian (Perch-Nielsen

1985; Bown 1998). Didemnoides moreti (Durand Delga) and

Globochaete alpina Lombard (Fig. 3) are also rarely present.

Limestones contain quartz clasts, muscovite leaflets and spo-

radic glauconite grains.

MFT-2: Packstones and grainstones

(biomicrite / biomicrosparite)

They form the upper part of the Podhorie Fm in the section

studied (interval M204–M224). They originate in calm circa-

littoral depositional environments (Arnaud-Vanneau 1980).

Limestones contain intraclasts and moderate- to well-sorted

peloids with rounded morphologies. Abundant bioclasts are

represented mostly by fragments of echinoids, bivalves,

planktonic foraminifers such as Hedber

gella trocoidea

(Gandolfi) (Fig. 4 J) and Ticinella primula Luterbacher,

Ticinella roberti (Gandolfi), Ticinella sp. (Fig. 4 I–J), Globi

gerinelloides bentonensis (Morrow) of the Ticinella primula

Zone indicate the Middle Albian by Premoli-Silva & Verga

(2004) (Figs. 2, 3). From benthic foraminifers, Turriglomina?

anatolica Altiner, Haplophragmoides aff. vocontianus Moullade,

Dentalina sp. and Valvulineria sp. can be observed.

MFT-3:Grainstones(biomicrosparite)

They represent the basal part of the Manín Fm (interval

M225–M235). These microfacies types, containing less

diverse assemblages of microfossils were assigned to the shal-

lower infralitoral environments with a constant, moderate to

strong hydrodynamism (Arnaud-Vanneau 1980). Bioclasts

reach larger sizes and are usually recrystalized. First occur-

rences of bivalves, partially rudist shell fragments and dama-

ged orbitolinids occur in association with small benthic

foraminifers (textularids, miliolids).

MFT-4: Grainstones and rudstones

(biosparitic/biosparruditic)

They form the upper part of the Manín Fm in the Manín

Straits section (interval M236–M282). This facies zone corre-

sponds to sediments deposited in infralittoral environments of

the inner platform domain which indicate high hydrodyna-

mics, and shallow water with reworking of bioclasts (Arnaud-

Vanneau 1980). Fragments of rudist shells of Caprinidae type

are dominant and associated with bivalves and gastropods.

The typical foraminiferal associations of these caprinid bea ring

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beds consist of well-rounded orbitolinids (Fig. 7A–D). Less

frequent constituents are represented by fragments of

gastropods, crinoids, bryozoans, small benthic foraminifers

(Miliolida sp., Textularia sp.) and rare planktonic fora minifers.

The orbitolinid fauna determined and assigned to the

Barremian by E. Köhler, was probably redeposited as indi-

cated by the fact that they are present in clasts (Fig. 7 E, F).

In the Manín Fm, several successive generations of carbo-

nate cement (Fig. 8), were identified with cathodolumines-

cence. The common types are dark red, orange and yellow

(Fig. 8 B, B’). Dark red cement predominates and represents

the oldest generation that crystallized in intergranular pore

spaces and replaced dissolved parts of detrital grains. Orange

carbonate cement is younger and precipitated in the remaining

pore spaces, within interboundary pores separating the brown

cement sparite crystals, and in dissolved contact zones between

detrital grains and dark red cement (Fig. 8 B, B’). Both dark

red and orange generations are represented by calcite assigned

by Boggs & Krinsley (2006) to eogenesis. Yellow cement

(Fig. 8 B, B’) is the brightest and the youngest generation of

carbonate, which crystallized at the stage of telogenesis

(Boggs & Krinsley 2006) in pores that remained after precipi-

tation of the two older cement generations. Carbonates are

affected by selective dolomitization (facies selective dolomiti-

zation, cf. Soreghan et al. 2000), typical of peritidal and shal-

low neritic facies zones.

Rudist assemblages

The entire corresponding beds (M237–M282) belong to the

Manín Fm and formed part of a reef to peri-reef facies zone.

The richest accumulations (beds M247–M255, about 2–4

metres thick) of rudist shell fragments (1–2 cm) represented

by Caprinidae (Caprina sp., Praecaprina sp., Offneria sp.)

wackestone/

packstone

(biomicrit

biomicrosparite

)

MFT

-1

Pseudothalmanninella

ticinensi

ticinensis

Zone

Innominat

Acme

Zone

MMM

rudist

reef

grainstone/

rudstone

(biosparite

biosparrudite)

MFT

-4

icinella

Zone

alvulineria

sp.

Colomisphaera

gigantea

icinella

roberti

245

280

275

270

265

260

255

250

240

235

230

225

220

215

210

205

200

195

190

grainstone/

rudstone

(biosparite

biosparrudite

)

MFT

-4

grainstone

(biomicrosparite)

MFT

-3

packstone/

grainstone

(biomicrit

biomicrosparite

)

MFT

-2

Butkov

Caprinidae

(

sp.

sp.)

Caprina

Praecaprin

Offneria

185

180

Haplophragmoide

vocontianus

urriglomina

anatolica

Dentalina

sp.

Akcaya

minuta

Colomiella

recta

Colomiella

mexicana

Globigerinelloides

bentonensis

icinella

praeticinensis
cf.

icinella

sp.

icinella

madecassiana
cf.

icinella

primula

enobulimina

sp.

Nannoconus

bucheri

atznaueria

barnesiae

etar

habdus

sp.

Calpionella

alpina

Bolivinopsis

capitata

Glomospir

ella

gaultina

Lor

enziella

hungarica

Anomalina

sp.

ondicularia

sp.

Mayncina

bulgarica

Colomiella

sp.

Globigerinelloides

sp.

Globochaete

alpina

Didemnoides

mor

eti

Cadosina

semiradiata

olzae

Lenticulina

sp.

Patellina

sp.

Spirillina

sp.

Meandr

ospira

favr

Gaudryina

sp.

Hedber

ella

sp.

Calcisphaerula

innominata

Crassicollaria

parvula

Palorbitolina

lenticularis

alserina

brönnimanni

Paleodictyonus

barr

emianees

Orbitolinopsis

sp.

Hedber

ella

ocoidea

Parathalmanninella

appenninica

Fig. 3. Litho- and biostratigraphy of the the Manín and Podhorie fms (for legend, see also Fig. 2). Crosses — redeposited microfossils,

dots — autochthonous microfossils.

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can originate in the deeper parts of the substrate in an environ-

ment with very low or without oxygen content that fosters

sulphate reduction (Bromley 1996). The calcisphaerulid layer

also contains thin (about 1 mm) rusty-brown burrows of

Trichichnus (Frey, 1970) and Pilichnus (Uchman, 1999). They

are branched or unbranched, hair-like, cylindrical, straight to

sinuous trace fossils, oriented at various angles (mostly verti-

cal) with respect to the bedding, and filled by pyritized mate-

rial. The producers of Trichichnus and Pilichnus were probably

also chemosymbionts that harboured small filamentous bacteria

in deeper portions of very poorly oxygenated sediments.

(Kędzierski et al. 2015).

According to microstructure, the studied limestones repre-

sent calcisphaerulid – foraminiferal micrite (calcisphaerulid –

foraminiferal wackestone / packstone). The microfacies is

calci sphaerulid or calcisphaerulid – foraminiferal. Allochems

are for the most part directed.

Based on abundant microfossils, the age of the calci-

sphaerulid limestone corresponds to the top of the Late Albian.

Planktonic foraminifers of the Parathalmanninella appenninica

Zone (e.g., Premoli Silva & Verga 2004) are represented by the

index form

Parathalmanninella appenninica

(Renz) (Fig. 10 A).

In addition, Planomalina buxtorfi (Gandolfi) (Fig. 10 F),

Pseudo thalmanninella ticinensis ticinensis (Gandolfi) (Fig. 10 D),

Pseudothalmanninella ticinensis conica (Gašpariková et Salaj)

(Fig. 10 B), Praeglobotruncana delrioensis (Plummer), Prae

globotruncana stephani (Gandolfi) (Fig. 10 C), Murico hed

bergella delrioensis (Carsey), Muricohedbergella planispira

(Tappan), Globigerinelloides caseyi (Bolli, Loeblich et Tappan)

(Fig. 10 H), Ticinella raynaudi (Sigal) (Fig. 10 I) and Hetero

helix sp. (Fig. 10 J) were identified. Benthic forami nifers are

rare, represented mostly by Nodosaria

sp. and Textularia sp.

Calcareous dinoflagellates are

repre sented by abundant Calci

sphaerula innominata Bonet

(Fig. 10 E) and by less frequent

Pithonella ovalis (Kauf mann)

(Fig. 10 J), Pithonella trejoi Bonet

(Fig. 10 E) and Bonetocardiella

conoidea (Bonet) (Fig. 10 F).

Cadosina oraviensis (Borza) and

Colomisphaera gigantea (Borza) of

the Innominata Acme Zone (assigned

to Late Albian by Reháková (2000)

are rare. Other fossil remains are rep-

resented by fragments of echinoids as

well as filaments,

thick-walled

bivalves and bioclasts. Phosphate

minerals, pyrite, rare authigenic

quartz (with undulose extinction) and

glauconite grains are present, some-

times filling shells and chambers of

foraminifers.

Geochemistry and magnetic susceptibility

The CaCO

content in the section ranges from 79.15 to

99.82 % (Fig. 11). In limestones of the Manín Fm (interval

M225 to M282), it remains constant and above 95 wt. %.

The CaCO

content decreases locally (99.80 % to 79.15 %) in

the Podhorie Fm. The CaCO

depletion could be connected

with a rise of silicate content (quartz, micas, glauconite) in the

sediments due to local tectonic processes. The TOC content

also slightly increased (by an average of 0.05 wt. %) in some

beds of the Podhorie Fm where CaCO

decreased (Fig. 11).

Generally, the TOC content is lower than 0.1 % in the samples

of the Manín Fm and documents nutrient pure regime on the

carbonate platform.

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

tively high variation: δ

C is in range +1.03 to +4.20 ‰ V-PDB

and δ

O is in range −0.14 to −5.55 ‰ V-PDB (Fig. 11).

The δ

C isotope data suggest shallow water realm and more

or less continuous diagenesis under marine conditions. Values

are comparable with other platform carbonates, especially

with Urgonian ones (Immenhauser et al. 2003; Godet et al.

2006; Föllmi & Godet 2013; Huck et al. 2013). The trends in

stable isotopes mirror the separation of the succession into

three intervals to some degree (the lower and upper parts of

the Podhorie Fm and the Manín Fm) (Fig. 11). The correlation

between δ

O versus δ

C trends indicate that a diagenetic

signal may dominate especially in the beds with significant

amount of sparite in the upper part of the sequence (Fig. 2). In

spite of diagenetic effect, isotope ratios of shallow-water

carbonates have a potential to record climatic changes and

changes in the burial of inorganic carbon in the platform realm

Fig. 8. Microfacies of the Manín Fm in optical (A, A’) and in cathodoluminiscence microscope

(B, B’). Photos are taken from sample No. M261.

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(Godet et al. 2006; Föllmi & Gainon

2008; Föllmi & Godet 2013).

The δ

C values in the range +2.19 to

+2.68 ‰ are typical of the lowermost part

of the section (M190–M203) formed by

bioclastic limestones with a relatively

high content of micrite matrix (wack-

stones), (Fig. 2). The wide range (−3.26 to

−0.14 ‰) and bed to bed shifts of δ

values (Fig. 11) indicate local changes in

the composition of sedimentary and/or

early diagenetic fluids. Less negative δ

values indicate that a saline water occa-

sionally penetrated into and/or was stored

in the platform sediment, which later

sourced sediments on the slope.

Thick-bedded and coarse-grained pack-

stones and grainstones of the Podhorie

Fm (M204–M224) are characterized by

initially decreasing (+1.03 ‰) and later

increasing (up to +4 ‰) δ

C trends. In

this part of the section, δ

O vary between

−1.61 and −5.55 ‰ but generally shift to

more negative values. Highly negative

O values could indicate fresh water

input to the sediment and/or meteoric

character of diagenetic fluids, and possibly

a more humid climate (Lackie et al. 2002;

Föllmi 2012).

In contrast to the Podhorie Fm, δ

values are higher and relatively uniform

(+3.52 to +4.20 ‰) in the Manín Fm

formed by bioclastic grainstones and rud-

stones (Figs. 2, 3). The δ

C decreased

(+3.19 to +3.17 ‰) just below the

hardground surface in beds M281 and

M282. The δ

O values shifted to mode-

rately negative values (−1.83 to −4.31‰)

and vary less than in the Podhorie Fm.

This indicates that the major volume of

the rock is formed by calcareous matter

derived from a platform and that primary

spary-cements precipitated from fluids

with isotopic composition similar to that

of marine water. An increase in humid

conditions with freshwater input may have preferentially

reduced the signature of δ

O on the platform (Poulsen et. al.

2007; Föllmi 2012).

MS values are mostly negative, between 0 and −6×10

-9

/kg,

indicating predominant influence of diamagnetic carbonate

rock matrix (Fig. 11). Exceptionally high values (54.7×10

-9

/kg) are observed only in a fault zone within the Podhorie

Fm (sample 205) and are most probably related to tectonic

phenomena. MS reveals a long term decreasing trend, from

occasionally positive values in the lower part of the Podhorie

Fm through −2 to −4×10

-9

/kg in the upper part of Podhorie

and lower part of the Manín Fm, to almost constant low values

of −4×10

-9

/kg in the upper part of the Manín Fm.

Discussion

Carbonate platform growth on Tethyan shelves has been

controlled by major eustatic and climatic fluctuations (Arnaud-

Vanneau 1980; Wissler et al. 2003; Weissert & Erba 2004).

During the Late Barremian to Early Albian, these shallow car-

bonate platforms were affected by major drowning episodes

Fig. 9. Manín Fm limestones. A–B: field photos — bed No. M254; C–D: Polished section.

The inner shell layer — white parts (primarily aragonitic) — is usually re-crystalized, dark

spots of prismatic calcite belong to the outer shell layer; E–F: microscopic photos — coarse-

grained organodetritic grainstone composed of poorly preserved caprinid rudists with a single

row of pyriform canals associated with large benthic foraminifera, samples No. M256,

M258.

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(Föllmi et al. 1994; Rosales 1999; Lehmann et al. 2000; Bièvre

& Quesne 2004; Yilmaz 2006). Collapse of the platforms was

accompanied by extensive submarine erosion and sliding of

extensive blocks (Ferry & Flandrin 1979; Michalík & Vašíček

1984; Schöllhorn & Schlagintweit 1990, etc.). Although the

age of platform carbonates of the Manín Unit outcropping in

the Manín Straits was assigned to the typical “Urgonian”,

Barremian–Aptian sequence in the Western Carpathians

mainly on the basis of orbitolinid and rudist assemblages

(Köhler 1980; Michalík & Vašíček 1984; Rakús 1984; Boorová

1991; Boorová & Salaj 1996), we show that the Podhorie and

Manín formations were deposited during the Albian.

Biostratigraphy and platform development

Biostratigraphic study of platform carbonates and associa-

ted basinal sediments show that the age estimates and litho-

logy of the platform sequence in the Manín Straits determined

in previous studies were inaccurate. Microfacies analyses and

age assignments based on distinctive assemblages of plank-

tonic foraminifers, calpionellids and calcisphaeres allow us to

restrict the demise of the carbonate platform to the Albian and

provide a schematic model displaying lithofacies architecture

and platform development similar to that proposed by Gili et

al. (2016), (Fig. 12). It can be assumed that the platform mar-

gin and upper slope sediments of the “Urgonian”, Barremian–

Aptian sequence, originally forming the higher highstand

platform have been eroded and their former slope was overlain

by lowstand platform exhibiting somewhat similar platform

margin and upper slope facies of the older highstand

platform.

The lowstand carbonate platform sequence in the Manín

Straits starts with upper slope facies of the Podhorie Fm with

cherts in the basal part. Based on planktonic foraminifers,

Calcisphaerula innominata which is known to occur in the

Albian (Borza 1969), Colomisphaera gigantea, tintinids

5.456 m /kg

-8

sample 205

90 100

0.1 0.2 0.3 0.4

-6

-5

-4

-3

-2

-1

C (‰ PDB)

O (‰ PDB)

CaCO

(%)

TOC (%)

-9

MS 10 m /kg

-8E-09

-6E-09

-4E-09

2E-09

4E-09

6E-09

8E-09

1E-08

-2E-09

70 80 90 100

0.1 0.2 0.3 0.4

-6 -5 -4

-3

-2 -1

-8E-09

-6E-09

-4E-09

2E-09

4E-09

6E-09

8E-09

1E-08

-2E-09

wackestone/

packstone

(biomicrite

biomicrosparite)

MFT

-1

Pseudothalmanninella

ticinensis

Zone

Innominata

Acme

Zone

MMM

rudist

reef

grainstone/

rudstone

(biosparite

biosparrudite)

MFT

-4

245

280

275

270

265

260

255

250

240

235

230

225

220

215

210

205

200

195

190

grainstone/

rudstone

(biosparite

biosparrudite)

MFT

-4

grainstone

(biomicrosparite

)

MFT

-3

packstone/

grainstone

(biomicrite

biomicrosparite)

MFT

-2

Butkov

icinella

Zone

Fig. 11. A scheme of stratigraphic division of the Manín and Podhorie fms in the Manín Straits section with fluctuation curves of δ

C and δ

isotopes, organic carbon content (TOC — Total Organic Carbon), calcium carbonate (CaCO

) and magnetic susceptibility.

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Colomiella recta and C. mexicana, these deposits correspond

to the Albian Ticinella primula Zone.

The Podhorie Fm passes upwards continuously into peri-

reef facies of the Manín Fm with significant accumulations of

rudist shell fragments, which can indicate renewed platform

progradation. With the exception of the study based on rudist

findings of Masse and Uchman (1997) from the High Tatra

Mts (Giewont, Wysoka Turnia, Hala Gąsienicowa) and from

the Muráň limestone named as the “Caprotinenkalk” by Uhlig

(1897 in Lefeld 1974), detailed taxonomic and biostratigraphic

studies of the Lower Cretaceous rudist faunas of the Central

Western Carpathians are absent. Investigations in the Manín

Straits document the existence of caprinid rudist shell frag-

ments. Their special status, uniqueness and character allow us

to designate the Malý Manín Member (beds M247–M255)

which has not been previously recognized and which has not

been defined at other localities of the Manín Unit. The fora-

miniferal association of these caprinid-bearing beds consists

predominantly of well-rounded orbitolinids. Some of them

occur in clasts from which they were “separated” by transport

into the limestones of the Manín Fm. Similar occurrences of

orbitolinid association were documented from other localities

in the Manín Unit (Boorová 1990, 1991). Signs of redeposi-

tion are also documented by the presence of rare pre-Albian

calpionellids and calcareous nannoplankton.

A sudden bathymetric collapse of the Manín carbonate plat-

form occurred during the Late Albian (Boorová 1990; Boorová

& Salaj 1992) and the environment has been affected by sub-

sequent low-rate sediment deposition. A hardground surface

described by Rakús (1984) probably originated in deeper

marine conditions with a minimum contribution of sediment.

This surface is overlain by marls and marlstones of the Butkov

Fm with an association of rare

benthic and current planktonic

foraminifers of the Late Albian

Thalmanninella ticinensis ticinen-

sis Zone (Boorová 1990). In the

Manín Straits, as well as on the

other localities of the Manín Unit

(Borza et al. 1983) a thin layer

(3–5 cm) of grey calcisphaerulid

limestone occurs just in the basal

part of the Butkov Fm. Based on

rich microfossil community, this

limestone was deposited during

the latest Albian.

Geochemistry

The δ

C record may be influen-

ced by different biological frac-

tionation of different groups of

calcareous plankton, different

types of mineralogy of pelagic

and benthic producers, by quan-

tity of organic carbon recycled,

and by diagenetic processes (Föllmi & Godet 2013). The δ

and δ

O values shift along the section in a close relation with

changes in the composition of microfacies and their tight cor-

relation suggests that they were subjected to diagenetic alte-

ration. However, the trend towards higher δ

C values within

the Manín Fm can suggest enrichment in the aragonite produc-

tion and/or isotopic composition of seawater dissolved inor-

ganic carbon (due to aragonite dissolution, higher nutrient

enrichment, and/or changes in the contribution of open ocea-

nic water mass and platform-top water masses). However,

local (tectonic) controls cannot be ruled out interpreting the

beginning and demise of carbonate depositional systems

(Ruberti et al. 2013; Sames et al. 2016).

The high δ

C values of the Manín Fm indicate that the main

amount of (sparitic-coarse) biodetrite comes from carbonate

platform and its edge, containing shells and mud with original

aragonite mineralogy. Input of non-carbonatic components in

the Manín Fm was generally low and identifiable by higher

values of MS. MS might have been influenced also by dis-

persed ferromagnetic and clay minerals that reside in the

micrite. A long term MS decrease is generally concordant with

upward-increasing CaCO

and sparite content (Figs. 2 and 11).

This trend most probably reflects a relative decrease of litho-

genic input. It is interesting that MS roughly follows the same

decreasing trend reflected in TOC (Fig. 11). Similarly as in the

case of the Urgonian facies of the Barremian–Early Aptian

age, the production of aragonite can be essential for a source

of the

C-heavy carbonate derived from the platform and

adjacent (peri-platform) basins (Föllmi et al. 2006; Godet et

al. 2006; Föllmi & Gainon 2008). In deep-water pelagic car-

bonates, positive shifts of δ

C resulted from enhanced burial

of the isotopically light sedimentary organic C (Weissert et al.

restricted

open lagoon

Platform

margin

Rudist

reef

Platform top facies

downslope

transport

Slope

facies

Basin marls

LST sea level drop

MF – Manín Formation PF – Podhorie Formation

erosion

BARREMIAN - APTIAN

ALBIAN

MFT1–
MFT4

Highstand platform

Lowstand platform

intertidal

supra-
tidal

Fig. 12. Schematic model displaying lithofacies architecture and platform development in the Manín

Straits. Based on Gili et al. (2016).

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AN ALBIAN DEMISE OF THE CARBONATE PLATFORM IN THE MANÍN UNIT (WESTERN CARPATHIANS)

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, 2017, 68, 5, 385–402

1998; Immenhauser et al. 2003, etc.). According to Immen-

hauser et al. (2003), a positive shift in δ

C (and δ

O) recorded

in lithified shallow-marine carbonates reflects a superposition

of environmental and diagenetic effects. During the transgres-

sion, the impact of isotopically light meteoric fluids on car-

bonate geochemistry is much reduced as indicated by higher

isotope values of shallow-water carbonates. Therefore, the

trend towards higher δ

C and δ

O can also reflect a decrea-

sing contribution of platform-top water masses towards the top

of the Manín Fm. In summary, the geochemical and sedimen-

tological trends within the Manín Unit suggest an overall

deepening at the site of sedimentation.

In the Manín Fm (peri-reef facies), sedimentary δ

C values

were affected by diagenesis as indicated by smooth trends of

the δ

C curve, and by high positive correlation (R

= 0.75)

between δ

O and δ

C. Non-identifiable recrystallized bio-

clasts and lithoclasts are cemented by calcite (spary calcites

— Fig. 2) that probably precipitated from pore waters of

marine origin. Variable δ

O values (−0.14 to −5.55 ‰, Fig. 11)

but low correlation between δ

O and δ

C (R

= 0.01) in lime-

stones of the lower part of the section (M191–M224, Podhorie

Fm) indicate differences in depositional and diagenetic condi-

tions between the Podhorie and Manín fms.

Frequent black shales in the mid-Cretaceous pelagic

sequence have been linked with anoxic bottom-water condi-

tions during Ocean Anoxic Events (1a–d), (Weisert et al. 1998;

Heimhofer et. al. 2008; Leckie et al. 2002; Kennedy et al.

2014; Giorgioni et al. 2015). Large fluctuations of the δ

signal were indicated in the pelagic sequences and local factors

such as productivity variations of surface water had an impact

on the carbon isotopic composition of deep water limestones

(Giorgioni et al. 2015; Ruberti et al. 2013). The local factors

are important in the sequence of shallow-water and temporally

isolated realm and global changes — for example, OAEs

recorded as C cycle perturbations may be specifically recorded

there (Föllmi et al. 2006; Godet et al. 2006; Föllmi & Gainon

2008; Ruberti et al. 2013).

The hardground indicates a demise of the mid-Albian

carbonate production. The basinal black shale with variable

carbonate and TOC contents were deposited over large areas

of the Mediterranean and the Atlantic Tethys (Ruberti et al.

2013). In this study, dysoxic conditions probably characte-

rized the deposition of marls, as indicated by trace fossils pre-

served in the calcisphaerulid limestone in the basal part of the

pelagic sequence. The demise of the mid-Albian platform may

be correlated with OAE 1c or OAE 1d (Leckie et al. 2002;

Ruberti et al. 2015).

Conclusions

The Albian carbonate platform sequence of the Manín Straits

exhibits peri-reef to upper slope facies of the older destroyed

Barremian–Aptian highstand platform. The sequence starts

with dark grey, thick-bedded to massive bioclastic limestones

of the Podhorie Fm, with cherts in the basal part. Albian age is

indicated by: (1) planktonic foraminifers of the Ticinella

primula Zone, colomiellids, Colomiella recta and C. mexicana,

and (2) calcareous dinoflagellates, Calcisphaerula innominata,

Colomisphaera gigantea and calcareous nannoplankton.

The Podhorie Fm passes upwards continuously into light grey,

massive, platform limestones of the Manín Fm with abundant

caprinid rudist shell fragments and a trend towards more posi-

tive δ

C where we designate the Malý Manín Member (beds

M247–M255). Their foraminiferal association consists of

well-rounded, redeposited orbitolinids.

Four dominant microfacies associations: bioclastic and

peloidal wackestones and packestones (MFT-1), packstones

and grainstones (MFT-2), bioclastic grainstones (MFT-3),

bioclastic grainstones and rudstones (MFT-4), (sensu Arnaud-

Vanneau 1980) allow us to restrict the growth and the demise

of the carbonate platform.

Isotopes in both formations change within wide intervals

(δ

C is in range +1.03 to +4.20 ‰ V-PDB and δ

O is in range

−0.14 to −5.55 ‰ V-PDB). Stratigraphic changes in δ

C in

the section indicate temporal changes in aragonite production

and/or in the isotopic composition of seawater dissolved inor-

ganic carbon, possibly due to reduced contribution of top-

platform water masses.

Carbonate platform evolution was connected with subma-

rine sliding, redeposition from older deposits, and carbonate

clast accumulation on the toe of the slope. After a stabilization

and aggradation stage, the carbonate platform collapsed just

prior to the Late Albian. A hardground surface was formed,

overlain by Albian–Cenomanian pelagic beds of the Butkov

Fm with a thin layer of calcisphaerulid limestone characte-

rized by planktonic foraminifers of the Parathalmanninella

appenninica Zone (top of the Late Albian) and calcareous

dinoflagellates of the Innominata Acme Zone.

Acknowledgements: The authors are grateful to E. Halásová,

S. Ozdínová, E. Köhler, S. Sano and Y. Salama for their

contribution and constructive comments. K. Švecová and

J. Leichmann for their assistance in preparing cathodolumi-

nescence records. This work was supported by UNESCO

IGCP 609, Slovak Grant Agency VEGA, projects

No. 2/0057/16, 2/0034/16 and the Slovak Research and

Development Agency, SRDA, project No. 14-0118. Construc-

tive reviews by an anonymous reviewers are greatly appre-

ciated.

References

Andrusov D. 1945: Geological research of the internal Klippen belt of

the Western Carpathians. Part IV. Middle and Upper Jurassic

stratigraphy. Part V. Cretaceous stratigraphy. Práce Štátneho

geologického Ústavu 13, 1–176.

Arnaud H., Arnaud-Vanneau A., Argot A. & Carrio C. 1995: Sequence

stratigraphy in a carbonate setting, platform to basin section of

the Urgonian platform (Lower Cretaceous), Vercors Plateau,

Glandasse Plateau to Isère Valley, Southeast France. AAPG,

Field Trip Notes, Nice, 14 –16 sept. 1995, 1–124.

400

FEKETE, SOTÁK, BOOROVÁ, LINTNEROVÁ, MICHALÍK and GRABOWSKI

GEOLOGICA CARPATHICA

, 2017, 68, 5, 385–402

Arnaud-Vanneau A. 1980: Micropaléontologie, paléoécologie et sédi-

mentologie d’une plate-forme carbonatée de la marge passive de

la Téthys. Géologie Alpine 11, 1–874.

Bièvre G. & Quesne D. 2004: Synsedimentary collapse on a carbo-

nate platform margin (Lower Barremian, southern Vercors, SE

France). Geodiversitas 26, 169–184.

Boggs S. Jr. & Krinsley H. 2006: Application of Cathodolumines-

cence Imaging to the Study of Sedimentary Rocks. Cambridge

University Press, Cambridge, UK.

Boorová D. 1990: Notes on the development of the Albian microfa-

cial development in the Belušské Slatiny (Manín Unit). In: Bio-

stratigraphical and sedimentological study of Mesozoic of Bohe-

mian Massif and Western Carpathians. Proceedings Hodonin:

Petroleum and natural gas industries, 169–182 (in Slovak).

Boorová D. 1991: Microfacies and microfauna of Upper Jurassic–

Lower Cretaceous Manín Unit. PhD thesis, Archive of SAS,

Bratislava, 1–224 (in Slovak).

Boorová D. & Salaj J. 1992: Remarks on the biostratigraphy on the

Butkov Formation in the Manín sequence. Geol. Carpath. 43, 2,

123–126.

Boorová D. & Salaj J. 1996: Contribution to the Barremian–Albian

litofacies development of the Manín Unit s. s. sediments. Zemní

plyn a nafta 40, 3, 177–184 (in Slovak).

Bom M.H.H., Guerra R.M., Concheyro A. & Fauth G. 2015: Methodo-

logies for recovering calcareous nannofossils from bituminous

claystone. Micropaleontology 61, 3, 165–170.

Borza K. 1969: Die Mikrofacies und Mikrofossilien des Oberjuras

und der Unterkreide der Klippenzone der Westkarpaten. Slovak

Academy of Sciences Publishing House, Bratislava, 1–302.

Borza K., Fedor J., Michalík J. & Vašíček Z. 1983: Lithology, strati-

graphy, tectonic conditions and chemical-technological charac-

teristics of cement materials from the Butkov Quarry. Interim

report on solving tasks. Open File Report — Geofond, Bratislava,

1–345 (in Slovak).

Borza K., Michalík J. & Vašíček Z. 1987: Lithological, biofacies and

geochemical characterization of the Lower Cretaceous palegic

carbonate sequences of Mt Butkov (Manín Unit, Western Car-

pathians). Geol. Carpath. 38, 3, 323–348.

Bown P.R. 1998: Triassic. In: Bown P.R. (Ed.): Calcareous nanno-

fossil biostratigraphy. British Micropalaeontological Society

Publication Series, Chapman & Hall, 29–33.

Bown P.R. & Young J.R. 1997: Mesozoic calcareous nannoplankton

classification. J. Nannoplankton Res. 19, 1, 21–36.

Bromley R.G. 1996: Trace fossils, biology, taphonomy and applica-

tions. Second edition. Chapman & Hall, 1–361.

Clavel B., Conrad M.A., Busnardo R., Charollais J. & Granier B.

2013: Mapping the rise and demise of Urgonian platforms (Late

Hauterivian–Early Aptian) in southeastern France and the Swiss

Jura. Cretaceous Res. 39, 29–46.

Dunham R.J. 1962: Classification of carbonate rocks according to

depositional texture. In: Ham W.E. (Ed.): Classification of car-

bonate rocks. A symposium. AAPG Memoirs 1, 108–171.

Erba E., Duncan R. A., Bottini C., Tiraboschi D., Weissert H., Jenkyns

H. C. & Malinverno A. 2015: Environmental Consequences of

Ontong Java Plateau and Kerguelen Plateau Volcanism. GSA

Special Paper 511, doi:10.1130/2015.2511(15).

Ferry S. & Flandrin J. 1979: Mégabrèches de resédimentation, lacunes

mécaniques et pseudo-“hard grounds“ sur la marge vocontienne

au Barrémien et à 1‘Aptien inférieur. Géol. alpine 55, 75–92.

Folk R.L. 1959: Practical petrographical classification of limestones.

AAPG Bulletin 43, 1–38.

Folk R.L. 1962: Spectral subdivision of limestone types. In: Ham

W.E. (Ed.): Classification of carbonate rocks. AAPG Memoirs 1,

62–84.

Föllmi K.B. 2012: Early Cretaceous life, climate and anoxia.

Cretaceous Res. 35, 230–257.

Föllmi K.B. & Gainon F. 2008: Demise of the northern Tethyan

Urgonian carbonate platform and subsequent transition towards

pelagic conditions: the sedimentary record of the Col de la Plaine

Morte area, central Switzerland. Sediment. Geol. 205, 142–159.

Föllmi K.B. & Godet A. 2013: Palaeoceanography of Lower

Cretaceous Alpine platform carbonates. Sedimentology 60,

131–151.

Föllmi K.B., Weissert H., Bisping M. & Funk H. 1994: Phospho-

genesis, carbon-isotope stratigraphy, and carbonate-platform

evolution along the Lower Cretaceous northern Tethyan margin.

Geol. Soc. Am. Bull. 106, 729–746.

Föllmi K.B., Godet A., Bodin S. & Linder F. 2006: Interactions

between environmental change and shallow water carbonate

build-up along the northern Tethyan margin and their impact on

the Early Cretaceous carbon isotope record. Paleoceanography

21, 1–16.

Frey R.W. 1970: Trace fossils of Fort Hays Limestone Member of

Niobara Chalk (Upper Cretaceous), West-Central Kansas.

The University of Kansas Paleontological Contributions 53,

1–41.

Fu S. 1991: Funktion, Verhalten und Einteilung fucoider und

lophocteniider Lenebsspuren. Courier Forsch. Inst. Sencken

berg 135, 1–79.

Gili E., Skelton P.W., Bover-Arnal T., Salas R., Obrador A. &

Fenerci-Masse M. 2016: Depositional biofacies model for post-

OAE1a Aptian carbonate platforms of the western Maestrat

Basin (Iberian Chain, Spain). Palaeogeogr. Palaeoclimatol.

Palaeoecol. 453, 101–114.

Giorgioni M., Weissert, H. Stefano M., Bernasconi, H.S., Hochuli

P.A., Keller C.E., Coccioni R., Petrizzo M.R., Lukeneder A. &

Garcia T.I. 2015: Paleoceanographic changes during the Albian–

Cenomanian in the Tethys and North Atlantic and the onset of

the Cretaceous chalk. Global Planet. Change 126, 46–61.

Godet A., Bodin S., Follmi K.B., Vermeulen J., Gardin S., Fiet N.

Addate T., Berner Y., Stúben D. & van de Schootbrugge V. 2006:

Evolution of the marine stable carbon-isotope record during the

early Cretaceous: A focus on the Hauterivian and Barremian in

the Tethyan realm. Earth Planet. Sci. Lett. 242, 254–271.

Heimhofer U., Adatte T., Hochuli P.A., Burla S. & Weissert H. 2008:

Coastal sediments from the Algarve: low-latitude climate archive

for the Aptian–Albian. Int. J. Earth Sci. 97, 785–797.

Huck S., Heimhofer U., Immenhause A. & Weissert H. 2013: Carbon

isotope stratigraphy of Early Cretaceous (urgonian) shoal-water

deposit: Diachronous changes in carbonate-platform production

in the north-western Thethys. Sediment. Geol. 290, 157–174.

Immenhauser A., Poter G., Kenter J.A.M. & Bahamonde J.R. 2003:

An alternative model for positive shift in shallow-marine car-

bonate δ

C and δ

O. Sedimentology 50, 953–959.

Kędzierski M., Uchman A., Sawlowicz Z. & Briguglio A. 2015:

Fossilized bioelectric wire – the trace fossil Trichichnus. Biogeo

sciences 12, 1–9.

Kennedy W.J., Gale A.S., Huber B.T., Petrizzo M.R., Bron P. &

Barchetta A. 2014: Integrated stratigraphy across the Aptian/

Albian boundary at Col de Pré-Guittard (southern France):

A Candidate Global Boundary Stratotype Section: Cretaceous

Res. 51, 248–259.

Köhler E. 1980: Stratigraphy of Cretaceous sediments based on Orbi-

tolinid foraminifers. The final report for the years 1976 –1980.

SGIDS, Bratislava, 1–91 (in Slovak).

Kysela J., Marschalko R. & Samuel O. 1982: Lithostratigraphic clas-

sification of Upper Cretaceous sediments of the Manín Unit.

Geologické Práce, Správy 78, 143–168 (in Slovak).

Leckie R.M., Bralower T.J. & Cashman R. 2002: Oceanic anoxic

events and plankton evolution: biotic response to tectonic

forcing during the mid-Cretaceous. Paleoceanography 17, 3,

doi: 10.1029/2001 PA 000623.

401

AN ALBIAN DEMISE OF THE CARBONATE PLATFORM IN THE MANÍN UNIT (WESTERN CARPATHIANS)

GEOLOGICA CARPATHICA

, 2017, 68, 5, 385–402

Lefeld J. 1974: Middle–Upper Jurassic and Lower Cretaceous bio-

stratigraphy and sedimentology of the Sub-Tatric succession in

the Tatra Mts. (Western Carpathians). Acta Geol. Polon. 24, 2,

227–364.

Lehmann C., Osleger D.A. & Montanez I.P. 2000: Sequence strati-

graphy of Lower Cretaceous (Barremian–Albian) carbonate

platforms of northeastern Mexico: regional and global correla-

tions. J. Sediment. Res. 70, 373–391.

Loeblich A.R. & Tappan H. 1988. Foraminiferal Genera

and their Classification. Van Nostrand Reinhold, 1–970

+ 847 pl.

Longoria J.F. 1974: Stratigraphic, morphologic, and taxonomic studies

of Aptian planktonic foraminifera. Revista Española de Micro

paleontología, número extraordinario, 1–107.

Longoria J.F. 1984: Cretaceous biochronology from the Gulf of

Mexico region based on planktonic microfossils. Micropaleon

tology 30, 225–242.

Masse J.P. 1989a: Relations entre modifications biologiques et

phénoménes géologiques sur les plates-formes carbonatées du

domaine périméditerranéen au passage Bédoulien-Gargasien.

Géobios, Mémoire Spécial 11, 274–294.

Masse J.P. 1989b: Biomineralization, mass extinctions and global

events relationships: mid-Aptian carbonate platform biota crisis

example. In: Abstracts, 28th International Geological Congress,

Washington 2, 382.

Masse J.P. 2003: Integrated stratigraphy of the Lower Aptian and

applications to carbonate platforms: a state of the art. In: Gili E.,

Negra M.H. & Skelton P.W. (Eds.): North African Cretaceous

Carbonate Platform Systems. NATO Science Series, IV. Earth

and Environmental Sciences 28. Kluwer Academic Publishers,

203–214.

Masse J.P. & Fenerci-Masse M. 2011: Drowning discontinuities and

stratigraphic correlation in platform carbonates. The late Barre-

mian–Early Aptian record of southeast France. Cretaceous Res.

32, 6, 659–684.

Masse J.P. & Fenerci-Masse M. 2013: Stratigraphic updating and cor-

relation of Late BarremianeEarly Aptian Urgonian successions

and their marly cover, in their type region (Orgon–Apt, SE

France). Cretaceous Res. 39, 17–28.

Masse J.P. & Uchman A. 1997: New biostratigraphic data on

the Early Cretaceous platform carbonates of the Tatra Moun-

tains, Western Carpathians, Poland. Cretaceous Res. 18,

713–729.

Masse J.P., Arias C. & Vilas L. 1992: Stratigraphy and biozonation of

a reference Aptian–Albian p. p. Tethyan carbonate platform suc-

cession: the Sierra del Carche series (oriental Prebetic zone —

Murcia, Spain). In: New aspects on Tethyan Cretaceous fossil

assemblages 9. Österreichische Akademie der Wissenschaften

Schriftenreihe der Erdwissenschaftlichen Kommissionen, Wien,

201–222.

Mello J. (Ed.) 2005: Geological map of the middle Váh Valley region

1:50,000. MŽP – ŠGÚDŠ, Bratislava.

Michalík J. 1994: Lower cretaceous carbonate platform facies, West-

ern Carpathians. Palaeogeogr. Palaeoclimatol. Palaeoecol. 111,

263–277.

Michalík J. & Soták J. 1990: Lower Cretaceous shallow marine build-

ups in the Western Carpathians and their relationship to pelagic

facies. Cretaceous Res. 11, 211–227.

Michalík J. & Vašíček Z. 1984: To the early mid-cretaceous deve-

lopment: the age and enviromental positionof the “Skalica

breccia”. Geologický zborník Geologica Carpathica 35,

559–581.

Michalík J. & Žítt J. 1988: Early Cretaceous phyllocrinids (Crinoidea,

Cyrtocrinida) in the Manín Unit (Mt Butkov, Middle Váh Valley,

Central West Carpathians). Geologický zborník Geologica

Carpathica 39, 3, 353–368.

Michalík J., Reháková D., Halásová E. & Lintnerová O. 2009: The

Brodno section — a potential regional stratotype of the Jurassic/

Cretaceous boundary (Western Carpathians). Geol. Carpath. 60,

3, 213–232.

Michalík J., Lintnerová O., Reháková D., Boorová D. & Šimo V.

2012: Early Cretaceous sedimentary evolution of a pelagic basin

margin (the Manín Unit, central Western Carpathians, Slovakia).

Cretaceous Res. 38, 68–79

Michalík J., Vašíček Z., Boorová D., Golej M., Halásová E., Hort P.,

Ledvák P., Lintnerová O., Měchová L., Šimo V., Šimonová V.,

Reháková D., Schlögl J., Skupien P., Smrečková M. &

Zahradníková B. 2013: The Butkov Hill, a stone archive of

Slovakian mountains and of the Mesozoic sea life history.

Veda Editorial house, Bratislava, 1–164. ISBN 978-80-224-

1287-2.

Michalík J., Reháková D., Grabowski J., Lintnerová O., Svobodová

A., Schlögl J., Sobień K. & Schnabl P. 2016: Stratigraphy,

plankton communities, and magnetic proxies at the

Jurassic / Cretaceous boundary in the Pieniny Klippen Belt

(Western Carpathians, Slovakia). Geol. Carpath. 67, 4, 303–328.

Mišík M. 1957: Lithological section through Manín series. Geolo

gický sborník 8, 2, 242–258 (in Slovak).

Mišík M. 1990: Urgonian facies in the West Carpathians. Zem. Plyn

Nafta, 9a, 25–54.

Perch-Nielsen K. 1985: Mesozoic calcareous nannofossils. In: Bolli

H.M., Saunders J.B. & Perch-Nielsen K. (Eds.): Plankton Stra-

tigraphy. Cambridge University Press, Cambridge, 329–426.

Peybernès B., Ivanov M., Nikolov T., Ciszaka R. & Stoykovac K.

2000: Séquences de dépôt à l’articulation plate-forme urgo-

nienne-bassin (intervalle BarrémieneAlbien) dans le Prébalkan

occidental (Bulgarie du Nord-Ouest). C. R. Acad. Sci. Paris,

Science de la terre et des planètes / Earth and Planetary Sciences

330, 547–553.

Plašienka D. & Soták J. 2015: Evolution of Late Cretaceous–

Palaeogene synorogenic basins in the Pieniny Klippen Belt and

adjacent zones (Western Carpathians, Slovakia): tectonic

controls over a growing orogenic wedge. Annales Societatis

Geologorum Poloniae 85, 1, 43–76.

Plašienka D., Havrila M., Michalík J., Putiš M. & Reháková D. 1997:

Nappe structure of the western part of the Western Carpathians.

In: Plašienka D. et al. (Ed.): Alpine evolution of the Western

Carpathians and related areas. D. Stur Publishers, Bratislava,

139–161.

Poulsen C.J., Pollard D. & White T.S. 2007: General circulation

model simulation of the δ

O content of continental precipitation

in the middle Cretaceous: a model-proxy comparison. Geology

35, 199–202.

Premoli Silva I. & Verga D. 2004: Practical manual of Cretaceous

Planktonic Foraminifera. In: Verga D. & Rettori R. (Eds.): Inter-

national school on Planktonic Foraminifera. Universities of

Perugia and Milano, Tipografia Pontefelcino, Perugia, 1–283.

Rakús M. 1984: Manín Straits-profile through the Jurassic and Creta-

ceous of the Manín nappe and profile at the Kostolec Klippe.

In: Guide to geol. excurs. West Carpath. Mts. Bratislava, 31–37.

Reháková D. 2000: Evolution and distribution of the Late Jurassic

and Early Cretaceous calcareous dinoflagellates recorded in the

Western Carpathian pelagic carbonate facies. Mineralia Slovaca

32, 2, 79–88.

Robaszyński F. & Caron M. 1995: Foraminiféres planctoniques du

Vrétacé: commentaire de la zonation Europe Méditerranée.

Société Géologique de France, Bulletin 166, 6, 681– 692.

Robaszyński F. & Caron M., coords., et Groupe de Travail Européen

des Foraminiféres Planctoniques 1979: Atlas de Foraminiféres

Planctoniques du Crétacé Moyen (Mer Boréale et Téthys).

Cahiers de Micropaléontologie, Paris, fasc. 1 et 2, 1–185 +

1–181.

402

FEKETE, SOTÁK, BOOROVÁ, LINTNEROVÁ, MICHALÍK and GRABOWSKI

GEOLOGICA CARPATHICA

, 2017, 68, 5, 385–402

Rosales I. 1999: Controls on carbonate platform evolution on active

fault blocks: the Lower Cretaceous Castro Urdiales platform

(Aptian–Albian, northern Spain). J. Sediment. Res. B. 69, 2,

447–465.

Ruberti D., Bravi S., Carannante G., Vigorito M. & Simone L. 2013:

Decline and recovery of the Aptian carbonate factory in the

southern Apennine carbonate shelves (southern Italy): Climatic/

oceanographic vs. local tectonic controls. Cretaceous Res. 39,

112–132.

Sames B., Wagreich M., Wendler J.E., Haq B.U., Conrad C.P.,

Melinte-Dobrinescu M.C., Hu X., Wendler I., Wolfgring E.,

Zilmaz I.O. & Zorina S.O. 2016: Review: Short-term

sea-level chcnges in a greenhouse world — a view from the

Cretaceous. Palaeogeogr. Palaeoclimatol. Palaeoecol. 441,

393–411.

Schöllhorn E. & Schlagintweit F. 1990: Allodapische Urgonkalke

(Oberbarreme-Oberapt) aus der Unterkreide-Schichtfolge der

Langbathzone (Nördliche Kalkalpen, Oberösterreich). Jb. Geol.

B.A. 133, 4, 635–651.

Simo J.A.T., Robert S.W. & Masse J.P. 1993: Cretaceous carbonate

platforms: an overview. In: Simo J.A.T., Roberts S.W. & Masse

J.P. (Eds.): Cretaceous Carbonate Platforms. AAPG Memoirs 56,

1–23.

Soreghan G.S., Engel M.H., Furley R.A. & Giles K.A. 2000: Glacio-

eustatic transgressive reflux, stratiform dolomite in Pennsylva-

nian bioherms of the western Orogrande Basin, New Mexico.

J. Sediment. Res. 70, 6, 1315–1332.

Štúr D. 1860: Bericht über die geologische Übersichts Aufnahme des

Wassergebietes der Waag und Neutra. Jahrb. Geol. Reichsanst, 9,

Wien, 17-151. In: Fusán O. 1960: Práce Dionýza Štúra —

vybrané state. Zpráva o prehľadnom geologickom mapovaní

v povodí Váhu a Nitry. GÚDŠ, Bratislava, 34–181.

Švábenická L. 2001: Late Campanian/Late Maastrichtian penetration

of high-latitude nannoflora to the Outer Carpathian depositional

area. Geol. Carpath. 52, 23–40.

Uchmann A. 1999: Ichnology of the Rhenodanubian Flysch (Lower

Cretaceous–Eocene) in Austria and Germany. Beringeria 25,

67–173.

Vašíček Z., Michalík J. & Reháková D. 1994: Early Cretaceous

stratigraphy, paleogeography and life in Western Carpathians.

Beringeria 10, 3–169 .

Weissert H. & Erba E. 2004: Volcanism, CO

and palaeoclimate:

a Late Jurassic–Early Cretaceous carbon and oxygen isotope

record. J. Geol. Soc. London 161, 695–702.

Weissert H., Lini A., Föllmi K.B. & Kuhn O. 1998: Correlation of

Early Cretaceous carbon isotope stratigraphy and platform

drowning events: a possible link? Palaeogeogr. Palaeoclimatol.

Palaeoecol. 137, 189–203.

Wilson J.L. 1975: Carbonate Facies in Geologic History. Springer

Verlag, New York, N.Y., 1–470.

Wissler L., Funk H.P. & Weissert H. 2003: Response of Early Creta-

ceous carbonate platforms to changes in atmospheric carbon

dioxide levels. Palaeogeogr. Palaeoclimatol. Palaeoecol. 200,

187–205.