GeolCarp_Vol55_No3_239

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RADIOLARIAN BIOSTRATIGRAPHY OF CENOMANIAN-TURONIAN SUBSILESIAN NAPPE

GEOLOGICA CARPATHICA, 55, 3, BRATISLAVA, JUNE 2004

239250

RADIOLARIAN BIOSTRATIGRAPHY OF THE

UPPER CENOMANIANLOWER TURONIAN DEPOSITS IN THE

SUBSILESIAN NAPPE (OUTER WESTERN CARPATHIANS)

MARTA B¥K

Institute of Geological Sciences, Jagiellonian University, Oleandry 2a, 30-063 Kraków, Poland; bak@ing.uj.edu.pl

(Manuscript received December 9, 2002; accepted in revised form October 2, 2003)

Abstract: The Upper Cenomanian-Lower Turonian flysch deposits of the Subsilesian Unit of the Outer Western

Carpathians include a characteristic interval of green and black, siliceous shales with manganese concretions, benthonites

and tuff, with abundant radiolarian fauna. Thirty two species of Radiolaria have been identified. Spherical cryptothoracic

and cryptocephalic Nassellaria dominate in the assemblage. Two radiolarian species: Alievium superbum and Crucella

cachensis have been proposed as biomarkers for setting the CenomanianTuronian boundary interval in the deposits of

the Subsilesian series of the Polish Outer Carpathians.

Key words: Cenomanian-Turonian boundary, Flysch Carpathians, Subsilesian Unit, Radiolaria.

Introduction

The Upper Cenomanian-Lower Turonian Green radiolarian

shales represent the most distinctive horizon of the Outer

Western Carpathians. They are present in the Skole Nappe

(so-called Do³he Formation), Silesian Nappe (the

Barnasiówka Radiolarian Shale Formation), Subsilesian

Nappe (Green radiolarian shales) and Magura Nappe (the

Hulina Formation) in the Polish part of the Outer Western

Carpathians. The thickness of these deposits varies from doz-

ens of centimeters to several meters in individual nappes.

They mainly consist of green shales with intercalations of

black, grey and olive, silty or calcareous shales, and they are

partly intercalated with green and red cherts and radiolarites.

Clastic intercalations are also present as thin-bedded, fine- and

very fine-grained sandstone. The lower part of the Green ra-

diolarian shales includes very characteristic layers of

ferromanganese concretions (documented only from the

Silesian and Subsilesian Nappes), and black shales with man-

ganese incrustations, known in all the nappes. Moreover, the

sediments of this age include benthonite intercalations and a

tuff layer (a few centimeters thick), situated just below the

layer with ferromanganese concretions.

The Upper Cenomanian-Lower Turonian deposits have

been a subject of biostratigraphical studies since the early

1930s. Previous authors dealing with micropaleontological

investigations focused their interests on foraminifers as the

most useful tool for biostratigraphical purposes (e.g. Liszkowa

1956, 1962; Liszkowa & Nowak 1962; Bieda et al. 1963;

Geroch et al. 1967; Geroch et al. 1985), however radiolarians

are the most abundant group in these deposits.

The aim of the present study is to precisely determine the

age of the Green radiolarian shales in the Subsilesian Nappe

on the basis of radiolarian fauna. A special interest was given

to the stratigraphic position of the ferromanganese concretions

level in relation to the Cenomanian-Turonian boundary.

History of study

Uhlig, who carried out his geological investigations in

Moravia, discovered the mid-Cretaceous deposits enriched in

radiolarians in 1888. The first attempt at an age assignment

was made by Sujkowski & Ró¿ycki (1930). These authors

correlated the variegated shales with radiolarian cherts (crop-

ping out in the Skole Nappe) with the radiolarite series of the

Southern Alps, the Western Apennines and the Pieniny

Klippen Belt. They assigned their age to the Late Jurassic on

the basis of lithological similarities with the above mentioned

deposits.

Later investigations were carried out in the Silesian Nappe,

where the Upper Cenomanian-Lower Turonian deposits are

much better exposed (Burtanówna et al. 1933; Nowak 1956;

Koszarski et al. 1959; Koszarski & Liszkowa 1963; Geroch

1967; Geroch et al. 1967, 1985; Gzik 1990; Gzik & Koszarski

1990; M. B¹k 1994, 2000; K. B¹k & M. B¹k 2000; K. B¹k et

al. 2001). The Early Albian age of the green shales with radi-

olarians in the Silesian series was suggested by Burtanówna et

al. (1933), based on the superposition between the Lgota Beds

and the Godula Beds. Koszarski et al. (1959) correlated the

green shales with radiolarians from the Silesian, Subsilesian

and Skole Nappes, and assigned them Cenomanian age, based

on a few globotruncanids (Silesian series).

Radiolarian fauna was used as a stratigraphic tool in the

early 1990s (M. B¹k 1994). Detailed studies were carried out

in the Silesian Nappe (Miêdzybrodzie section near Sanok),

where the radiolarian assemblage was correlated with the

Cenomanian radiolarian Holocryptocanium barbuiHolocrypto-

canium tuberculatum Zone. The study of radiolarians was also

made in other sections of the Silesian Nappe (M. B¹k 2000),

where the Late CenomanianEarly Turonian biozonation was

proposed for these deposits.

Recently, the Upper Cenomanianlowermost Turonian de-

posits in the Silesian Nappe have been distinguished as a for-

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mal lithostratigraphic unit, the Barnasiówka Radiolarian

Shale Formation (B¹k et al. 2001). Its detailed stratigraphic

position has been identified on the basis of the radiolarian

fauna and deep-water agglutinated foraminifers.

The Upper Cenomanian-Lower Turonian deposits, en-

riched in radiolarians, are poorly exposed in the Subsilesian

Nappe. One of the known localities is situated at Zasañ near

Mylenice (Fig. 1). The age of the deposits cropping out here

was previously determined as Albian on the basis of the cor-

relation with the Silesian and Skole series (Liszkowa in:

Burtan & Turnau-Morawska 1978). Lately, Gedl & M. B¹k

(2000) suggested a latest CenomanianEarly Turonian age on

the basis of dinocysts and radiolarian assemblages.

Geological setting

The Subsilesian series forms one of the Tertiary thrust-

sheets of the Outer Western Carpathians. Its exposed part is

represented by deposits of the Lower Cretaceous to Miocene

age. The paleogeographic position of the Subsilesian Basin is

interpreted as one of the subbasins of the Outer Carpathian

basin, situated south of the North European plate on the sub-

marine ridge, between the Silesian and Skole Subbasins

(Ksi¹¿kiewicz 1962).

Nowadays, the Subsilesian Nappe occurs in the Polish part

of the Western Carpathians as two parallel zones west of the

Dunajec River (Fig. 1). The northern zone is visible to the

north of the Silesian Nappe, between Brzesko and Cieszyn.

The southern zone appears in a few tectonic windows be-

tween the Dunajec and Skawa Rivers and in the ¯ywiec De-

pression. The studied section is located in the Mylenice

Fig. 1. Location of the section studied in the geological map of the

Outer Western Carpathians (after ¯ytko et al. (1988) simplified).

Abbreviations: Sk Skole Unit, Zg Zg³obice Unit, D + G

undivided Dukla and Grybów Units, G Grybów Unit, Zas lo-

cation of Zasañ section.

tectonic window, within the southern zone of the Subsilesian

Nappe. The window is built of a few tectonic slices with highly

tectonized Lower and Upper Cretaceous deposits.

The Albian-Turonian deposits of the Subsilesian Nappe

(Fig. 2) in this area are represented by the Gaize Beds (mainly

spongiolites with shale and siltstone intercalations), the Green

radiolarian shales (highly correlative to the Barnasiówka Ra-

diolarian Shale Formation from the Silesian Nappe) and the

lower part of the Variegated Shales (red and green shales

with single sandstone intercalations).

The studied section is situated at Zasañ settlement, near the

Trzemenia village, about 10 km east of Mylenice town. The

Gaize Beds do not crop out in the Zasañ section. The section

includes sediments correlated with the Barnasiówka Radiolar-

ian Shale Formation. It includes here (Fig. 3) green non-calcare-

ous shales intercalated by black non-calcareous shales, and

occasionally by green, pale green and spotty shales, partly cov-

ered by jarosite. Manganese shales with a layer of ferro-

manganese concrections (23 cm of diameter) occur higher up

in the section. A few layers of thin benthonite intercalate them.

One of the benthonite layers occurs just above the manganese

shale. The manganese series with benthonites represents the

middle part of this sequence. The higher part of the section

studied is represented by: (1) thin layers of green radiolarian

shales with ferrous coats intercalated with tuffites and

benthonites, (2) light grey and light blue highly siliceous

shales, with single intercalations of thin black shales and

gaizes (thin- to medium-grained sandstones enriched in sponge

spicules), and (3) green, blue-green and light grey clayey

shales intercalated with light grey and black siliceous shales.

Methods

Twenty eight samples have been collected from the studied

section. Radiolarians were extracted using two methods. Sili-

ceous shales were treated with 35% hydrofluoric acid. Clayey

Fig. 2. Lithostratigraphy of the Cenomanian through Turonian de-

posits in the Subsilesian Unit (after Koszarski & l¹czka 1973).

242

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shales and benthonites were boiled in diluted Glaubers salt.

The samples were sieved and the >63 µm fraction was exam-

ined. Selected samples with moderately to well-preserved ra-

diolarians were studied under the scanning electron

microscope (SEM), and the common faunal association is

documented in Table 1 and Figs. 47.

Radiolarian fauna is abundant in all samples but, in general,

poorly preserved, with few moderately to well-preserved

specimens. In some cases a relatively intense recrystallization

occurs. The poor preservation does not allow a statistical

evaluation of the fauna because the assemblage composition

and the differences reflect preservation rather than primary

faunal composition. Nevertheless, enough specimens are suf-

ficiently preserved for biostratigraphic analysis.

Table 1: Occurrence of the radiolarian specimens and local radiolarian zones in the Zasañ section.

Radiolarian assemblage

The radiolarian association comprises twenty taxa of

Spumellaria and twelve taxa of Nassellaria. According to the

systematic framework of ODogherty (1994) and Dumitricã

(1995) radiolarian taxa belong to six families of the order

Spumellaria and five families of the order Nassellaria.

Spumellaria include the following families and genera:

Pseudoaulophacidae (genera Alievium, Pseudoaulophacus

and Patellula), Patulibracchidae (genera Paronaella and

Halesium), Actinommidae (genus Praeconocaryomma), Orbi-

culiformidae (genus Crucella), Cavaspongiidae (genus Cava-

spongia) and Pyramispongidae (genus Pyramispongia). Nas-

sellaria are mainly represented by Williriedellidae (genera

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RADIOLARIAN BIOSTRATIGRAPHY OF CENOMANIAN-TURONIAN SUBSILESIAN NAPPE

Cryptamphorella, Hemicryptocapsa and Holocryptocanium),

other species belong to the families Diacanthocapsidae (genus

Diacanthocapsa), Archaeodictyomitridae (genus Dictyomi-

tra), Pseudodictyomitridae (genus Pseudodictyomitra), and

Amphipyndacidae (genus Stichomitra).

The analysed assemblage is dominated by spherical cryp-

tothoracic and cryptocephalic Nassellaria, belonging mostly

to the species Holocryptocanium barbui Dumitricã and Ho-

locryptocanium tuberculatum Dumitricã. These species repre-

sent 6099 % of the whole assemblage. Spumellarians are less

common but more diversified. As the number of species, they

represent up to 40 % of the radiolarian fauna.

Radiolarian biostratigraphy

Sixteen samples yielding radiolarians were studied from the

interval investigated. The results are presented in Table 1.

Biostratigraphically important species include Alievium su-

perbum (Squinabol), Crucella cachensis Pessagno, Patellula

ecliptica ODogherty, Patellula andrusovi Ovoldová, Holo-

cryptocanium barbui Dumitricã, Holocryptocanium tubercu-

latum Dumitricã, Pyramispongia glascockensis Pessagno,

Cavaspongia antelopensis Pessagno, Paronaella californi-

aensis Pessagno, Crucella messinae Pessagno, Stichomitra

communis Squinabol, Praeconocaryomma universa Pessag-

no, Praeconocaryomma lipmanae Pessagno, Pseudodictyomi-

tra pseudomacrocephala (Squinabol), Diacanthocapsa

euganea Squinabol, Dictyomitra napaensis Pessagno,

Pseudoaulophacus putahensis Pessagno, Dictyomitra undata

Squinabol, Pseudoeucyrtis pulchra (Squinabol), Patellula

cognata ODogherty, Paronaella communis (Squinabol),

Cavaspongia euganea (Squinabol) and Cavaspongia sphaeri-

ca ODogherty. This association is characteristic of the fauna

around the Cenomanian-Turonian Boundary Event (CTBE),

well described both from oceanic and land sections, for exam-

ple, from the Pacific: Moore (1973), Foreman (1975); Atlantic

Ocean: Thurow (1988); Carpathians: Dumitricã (1975), M.

B¹k (1999a,b); Mediterranean: Marcucci et al. (1991),

ODogherty (1994); Japan: Taketani (1982); Caucasus: Vish-

nievskaya (1993); Russian Pacific Rim: Vishnievskaya

(1993); California: Pessagno (1976).

Several species occurring in the studied radiolarian assem-

blage are not influenced by the CTBE (long-ranging forms).

These include Halesium amissum (Squinabol), Holocryptoca-

nium barbui Dumitricã, Holocryptocanium tuberculatum

Dumitricã, Pyramispongia glascockensis Pessagno, Patellula

helios (Squinabol), Patellula verteroensis (Pessagno),

Pseudodictyomitra pseudomacrocephala (Squinabol), and

Stichomitra communis Squinabol. On the other hand, the

CTBE is reflected in disappearance (LO) and the first appear-

ance (FO) of some radiolarian species.

Crucella messinae Pessagno is one of the species which has

its LO in the CTBE deposits. Its LO in uppermost Cenoma-

nian is reported, from the California Coast Ranges (Pessagno

1976), Northern and Central Italy (Erbacher 1994), Northern

Atlantic (Thurow 1988; Erbacher 1994) and elsewhere. Ac-

cording to ODogherty (1994) the last appearance data (LAD)

of C. messinae, calculated on the basis of the unitary associa-

tion method, took place in the earliest Turonian. In the studied

section, this species has its LO about 1.1 m below the ferro-

manganese concretions level (sample Zas-23). It coincides

with the first occurrences of Paronaella californiaensis Pessa-

gno, Patellula ecliptica ODogherty, Patellula andrusovi

Ovoldová and Praeconocaryomma universa Pessagno, spe-

cies which make their FOs in the CTBE.

Other important species for radiolarian biostratigraphy with

relation to the Cenomanian-Turonian boundary (CTB) are

Alievium superbum (Squinabol) and Crucella cachensis Pes-

sagno. In the Zasañ section, A. superbum appears in the high-

est part of the green shales (sample Zas-6), about 3.4 m above

the ferromanganese concretions level. The FO of C. cachensis

(sample Zas-7) is noted 0.5 m below the FO of A. superbum.

Both species have their FAD very close to the CTB e.g., Pes-

sagno (1976; Schaaf 1985; Thurow 1988). The authors men-

tioned above used these taxa to define the radiolarian A.

superbum Zone, the lower boundary of which coincides with

the CTB.

Pessagno (1976) was the first to discuss the FAD of A.

superbum in the Boreal Province of the California Coast

Ranges in relation to the CTB. According to this author, the

lower part of A. superbum Zone lies in the lower part of the

Inoceramus labiatus Zone, close to its lower limit and could

also coincide with the first appearance of double-keeled Glo-

bigerinacea (Helvetoglobotruncana helvetica).

Recently, the Cenomanian-Turonian boundary was pro-

posed in 1996 during the Second International Symposium on

Cretaceous Stage Boundaries in Brussels. It coincides with

the FO of the ammonite Watinoceras devonense at the base of

Bed 86 in the stratotype section at Rock Canyon Anticline,

west of Pueblo (Colorado). According to the inoceramid

biozonation (see compilation made by Bengtson 1996) and

ammonite zonations (Kennedy & Hancock 1976 and Kennedy

et al. 1983; compiled by Robaszynski 1983), the lower part of

the I. labiatus Zone coincides with the lower part of the

Watinoceras coloradoense Ammonite Zone. The lower limit

of the ammonite W. coloradoense Zone in Europe

(biozonation of Cobban et al. 1994 and Obradovich 1993 in:

Gradstein et al. 1995) could conceivably be correlative with

the lower boundary of the Watinoceras devonense Zone of

North America. The FO of W. coloradoense is placed in the

stratotype section within Bed 97 (1.5 m above the base of W.

devonense) (Kennedy & Cobban 1991). H. helvetica appears

(FAD) less than 1 m above the base of Bed 86 in the

stratotype section. In summary, according to the correlation

presented above, the first appearance (FAD) of A. superbum

could conceivably take place 11.5 m above the present

Cenomanian-Turonian boundary.

Crucella cachensis Pessagno is another radiolarian species,

which appears very close to the CTB. According to previous

investigations (Górka 1996; M. B¹k 2000; Gedl & B¹k 2000;

K. B¹k et al. 2001), this species is common in the Outer West-

ern Carpathian deposits. The species first occurs in the studied

section 0.5 m below the FO of A. superbum (sample Zas-7).

The previous workers reported the presence of C. cachensis

exclusively within the CTBE deposits (Ibiden). Thurow

(1988) proposed a radiolarian Crucella cachensis Zone for the

Northern Atlantic based on the first occurrence of the index

248

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species. He noted that this species never occurs with plank-

tonic foraminiferal species of the genus Rotalipora and its FO

is always coeval with the onset of the planktonic foraminiferal

Whiteinella aprica Zone.

In summary, both radiolarian species A. superbum and C.

cachensis, present in the siliceous deposits of the Subsilesian

series, are very useful biomarkers for placing the lower

boundary of the Turonian. They make their FOs above the fer-

romanganese concretion level. Consequently, the stratigraphi-

cal position of the ferromanganese concretion level is within

the uppermost Cenomanian.

Radiolarian correlation

The studied radiolarian assemblage, including all radiolari-

ans recovered in the deposits of the Subsilesian Nappe, has

been used for comparison with radiolarian zonal schemes

from different regions, especially from the Carpathians and

Mediterranean.

The radiolarian association from the lower part of the Zasañ

section (below the FO of C. cachensis and A. superbum) cor-

relates well with the Holocryptocanium barbui-Holocrypto-

canium tuberculatum assemblage proposed by Dumitricã

(1975) for the radiolarian-bearing deposits of the Romanian

Carpathians. This radiolarian assemblage shows great similar-

ity with the association presented herein, based on the co-oc-

currence of H. barbui and H. tuberculatum, and other

cryptocephalic and cryptothoracic Nassellaria. Moreover,

some multi-segmented Nassellaria from the genera Dictyomi-

tra, Pseudodictyomitra and Stichomitra also occur together. A

high percentage of cryptothoracic and cryptocephalic Nassel-

laria, especially H. barbui and H. tuberculatum is one of the

outstanding features of the radiolarian assemblages from the

Late Cenomanian to Early Turonian interval in the Car-

pathians. This feature has been reported from many sections

investigated in the Polish Outer Carpathians: in the Silesian

(M. B¹k 1994, 2000; K. B¹k et al. 2001) and Skole Units

(Górka 1996). It is also character of the radiolarian assem-

blages reported from all successions in the Polish part of the

Pieniny Klippen Belt (M. B¹k 1993, 1995, 1996a,b, 1999a,b).

The FO of A. superbum in sample Zas-6 marks the base of

the radiolarian Alievium superbum Zone of Pessagno (1976),

which includes the radiolarian assemblage from the upper part

of the section. This radiolarian biozone was also recognized in

the Mediterranean region (superbum Zone of ODogherty

1994). The A. superbum Zone can be well distinguished only

in the Outer Western Carpathians (Subsilesian, Silesian and

Skole Units). In the Slovak part of the Pieniny Klippen Belt,

the species A. superbum has been found only within the

Czorsztyn Succession (Sýkora et al. 1997).

This interval is also well correlated with the radiolarian

Crucella cachensis Zone of Thurow (1988) distinguished in

the North Atlantic. ODogherty (1994) also reported Crucella

cachensis from the Mediterranean region. This species is

common in the Outer Carpathian deposits, especially in the

Subsilesian and Skole Nappes, but it is rare in the Polish part

of the Pieniny Klippen Belt. Up to now, it has been found

only within the superbum Zone in the Czorsztyn Succession

in the Slovak part of the Pieniny Klippen Belt (Sýkora et al.

1997).

Conclusions

The results presented here are based on micropaleontologi-

cal analysis of twenty-eight samples collected from one sec-

tion (Zasañ section) of mid-Cretaceous deposits of the

Subsilesian Unit, in its Polish part. The studied deposits are

very rich in radiolarians. Lithologically, they consist mainly

of green shales with black shale intercalations, including man-

ganese concretions level, benthonites and tuff layers. These

deposits represent a characteristic correlation horizon, present

in the whole Carpathian arc.

A systematic study of all radiolarian species occurring in

the investigated samples allowed us to evaluate the diversity

of the radiolarian fauna. Twenty species of Spumellaria and

twelve species of Nassellaria have been recognized. The radi-

olarian assemblage is dominated by spherical cryptocephalic

Nassellaria, belonging mainly to the species Holocryptocani-

um barbui Dumitricã and H. tuberculatum Dumitricã. These

species make up 60 to 99 percent of the assemblage. Spumel-

larians are less common but more diversified. They represent

up to 40 percent of the radiolarian fauna, and are represented

mainly by the genera Patellula, Crucella, Paronaella, Prae-

conocaryomma and Alievium. This association is characteris-

tic of the fauna around the Cenomanian-Turonian Boundary

Event (CTBE).

Two radiolarian species: Alievium superbum (Squinabol)

and Crucella cachensis Pessagno, present in the siliceous de-

posits of the Subsilesian series have been used as biomarkers

to place the Lower Turonian boundary. They make their first

occurrence above the ferromanganese concretions level (A.

superbum 3.4 m and C. cachensis 0.5 m). Consequent-

ly, the age of the ferromanganese concretion level was deter-

mined as the uppermost Cenomanian.

All radiolarian taxa recorded in the studied deposits have

been used for comparison with the radiolarian zonal schemes

of previous authors in different areas of the Carpathians and

the Mediterranean Basin.

Acknowledgments: Thanks are due to Assoc. Prof. J. Michalík,

Dr. L. Ovoldová, Dr. P. Dumitricã, and Dr. L. ODogherty

for their critical review of the manuscript. Mrs J. Faber is

gratefully acknowledged for her technical assistance in photo-

graphing the identified fauna.

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