Foraminiferal biostratigraphy of the Albian and Cenomanian sediments in the Polish part of the Pieniny Klippen Belt, Carpathian Mountains

Cretaceous

Research

{ 1988) 9, 2 17-247

Foraminiferal biostratigraphy of the Albian and Cenomanian sediments in the Polish part of the Pieniny Klippen Belt, Carpathian Mountains. M. A. Gasiiiski Institute of Geological

Sciences,

Received

1987 and accepted

9 September

Jagiellonian

University,

2.5 April

Oleandry

2a, 30-063

Cracow,

Poland

1988

Seven local biostratigraphic zones have been distinguished in the Albian and Cenomanian sediments of the Pieniny Klippen Belt: Hedbergellu assemblage (Assemblage Zone, AZ), I?. R. ticinensis- P. praebuxtorfi subticinensis-R. ticinensis (Concurrent Range Zone, CRZ), (CRZ), R. tic&en& P. buxtorfi (Partial Concurrent Range Zone, PCRZ), P. buxtorfi- R. appenninica (CRZ), R. appenninica (Partial Range Zone, PRZ) and R. reicheli- R. greenhornensis (PCRZ), The zones are tentatively correlated with the ortho- and parastratigraphic zones of the Albian and Cenomanian. Three palaeoecological associations have been shelf-upper slope, large proportion of nodosarids and miliolids; distinguished: “Czorsztyn”, “Pieniny A” middle part of slope, oligotaxic planktonic assemblages dominant; “Pieniny B”, of agglutinated foraminifers. All fall depth similar to that of “Pieniny A”, larger proportion within the “_?Lfarssonella” association sensu Haig (1979). Layers of black shales, interpreted to reflect Cretaceous oceanic anoxic events, are correlated between successions of the Pieniny Klippen Belt, and their biostratigraphical position is determined. KEY WORDS: foraminifers, ecology, anoxic events.

1.

Albian,

Cenomanian,

Vraconian,

biostratigraphy,

palaeo-

Introduction

The Pieniny Klippen Belt is a zone of strongly deformed Mesozoic and Palaeogene rocks situated at the boundary between the Inner and Outer Carpathians (Figure 1). It is nearly 600 km long and only rarely exceeds a few kilometres in width. Its structure is dominated by rigid limestone klippen embedded in tightly deformed more competent strata; mainly marls, shales and flysch. Moreover, fragments of Outer and Inner Carpathian units are tectonically incorporated into this complex structure. Since the pioneering paper by Ksigikiewicz (1958) on the foraminiferal biostratigraphy of the Upper Cretaceous sediments in the Pieniny Klippen Belt, several authors have dealt with the stratigraphy and micropalaeontology of these deposits (Alexandrowicz, 1966, 1979; Alexandrowicz et al., 1962, 1968a, b; Birkenmajer & Geroch, 1961; Jednorowska, 1979, 1980; Scheibnerova, 1969, and others). Albian and Cenomanian sediments in the Polish part of the belt contain abundant and well-preserved foraminifers, including numerous planktonic index species. Earlier studies have already shown that precise biostratigraphic zones may be distinguished on the basis of foraminifers in the southernmost facies (Gasihski, 1983). Their good O19.G6671!030217+31

$03.00/O

(’ 1988 Academic Press Limlfed

218

X1. A. Gasiliski

preservation has permitted detailed description of test morphology and ultrastructure, and their abundance has enabled inferences to be made on the intraspecific variation of some species (Gasinski, 1981, 1983, 1984). These promising early results stimulated the author to prepare a detailed study of foraminifers in all facies and structural zones in the Polish part of the belt. However, only a few sections display almost complete sequences of the Albian-Cenomanian sediments and macrofauna is very scarce in these. Foraminifers (this paper) and calcareous nannoplankton (Dudziak, 1979, 1981) are the only index fossils. Moreover, the strata are indivisible by magnetostratigraphy because they are within a magnetic long normal zone (Figure 7. Quiet Zone: cf. Pialli 1977; Lowrie & Alvarez, 1977; Harland et al., 1982; Reyment & Bengtson, 1986). This paper is a contribution to IGCP Projects 198, “Evolution of the Northern margin of the Tethys”, and 262, “Tethyan Cretaceous Correlation”. Some of the results presented were demonstrated during field trips of the 57th Annual Meeting of the Polish Geological Society in the Pieniny 1986. Other less complete sections of Mountains during September, Albian-Cenomanian strata in the Pieniny Klippen Belt studied by the author but not included in this paper, are described in the excursion guidebook prepared for the meeting (Przewodnik, 1986). The foraminiferal assemblages are compared with material from the southern Alps and the Cmbria-Marche Apennines. A direct result of the

Figure 1. A. Sketch of part of the geological map of Poland (not including the Quaternary) c. 1:700 000 (after Ed. Wydawnictwa Geologicme, 1977). 1, I nner Carpathians: 2, Podhale Flysch; 3, Pieniny Klippen Belt; 4. Flysch of Magura Unit not subdivided Outer Carpathians; 5, Inner Carpathians, clays with lignites, sands and pebbles. B. Location of the studied sections; 1, Falsztyn; 2, Czorsztyn Castle; 3, Halka; 4, KapuQnica; 5, Cisowiec.

Biostratigraphy

of the Pieniny

Klippen

219

Belt

detailed biostratigraphic analysis is that black shale intercalations found in them and referred to the Cretaceous anoxic events can now be precisely located. 2.

Geological

setting

During late Mesozoic time the depositional basin of the Pieniny Klippen Belt belonged to the eastern (Alpine-Carpathian) branch of the Tethys Ocean. Several longitudinal facies zones, corresponding to troughs and ridges in the depositional basin, are distinguished in the cross section of the belt (Figure 2). Each has a distinctive lithostratigraphic succession (Birkenmajer, 1977, 1979, 1986). Several transitional zones of regional extension are distinguished between them. 3.

Sections

studied

Five sections were selected for detailed study of the Albian-Cenomanian foraminiferal assemblages. These are the formation stratotypes (Birkendisplaying almost complete sequences of the majer, 1977) and sections Albian-Cenomanian sediments. Three were exposed and studied in trenches because of the lack of sufficient natural outcrops.

1. Falsztyn ation,

Figure

(Czorsztyn succession, 3; Birkenmajer, 1963).

stratotype

of the Pomiedznik

Form-

This section is situated about 5 km west from the Niedzica Castle (Figure 1) and is a trench exposure. Attempts at improving the exposure of the lower

cenomanian

Jaworki Pomedml

ALbian

*

Fm

Marl

Kapufnlca

Fm Fm.

___

Aptian

N

Mg

Pieniny

/C/Q/N/B/

Lmst. Fm __I

P

Jo

c

Palinspastx reconstruction of the sedimentary basin of the Pieniny Klippen Belt during the Figure 2. Cenomanian, and mid-Cretaceous lithostratigraphical units (compiled after Birkenmajer, 1977, 1986). Mg, Magura basin, Outer Carpathians. Successions of the Pieniny Klippen Belr: C. Czorsztyn; Cz, Czertezik; N. Niedzica; B. Branisko; P. Pieniny; H. Haligowce. 1, continental crust; 2, oceanic crust; 3, carbonates and radiolarian cherts; 4, mantle; 5, flysch.

220

M. A. Gasiriski

SSE

NNW

0

I

Figure 3. 1963).

1

1

2

I

3

L

4

1

5m

I

Falsztyn section (Czorsztyn succession) exposed in trench (based mainly on Birkenmajer, SoL. Spisz Limestone Formation, crinoidal limestone (Valanginian-Hauterivian); Ch.

Chmielowa Formation. red marly limestone; PI. lower part of the Pomiedznik Formation, greyishgreen marly shales and marls alternating with light green marly limestones and cherts; Pu, upper part of the Pomiedznik Formation, marly shales and marls without cherts, black shales-sediments related to anoxic events; numbers refer to location of samples.

Jaworki Marl Formation in the uppermost part were unsuccessful. The Sprsz Limestone, Chmielowa and Pomiedznik Formations were examined here. A poorly stratified crinoidal limestone of the Spisz Limestone Formation (Valanginian-Hauterivian) underlies the studied part of the section, and is separated from it by a hiatus. The Chmielowa Formation (Albian) consists of thin-bedded, red marly limestones which are nodular in part. They are strongly fissile parallel to the bedding planes. Upwards, the Chmielowa Formation is transitional to the Pomiedznik Formation. The lower part of the latter consists of thin-bedded, greyish-green marly shales and marls, alternating with thin layers of light green marly limestones. Thin layers of dark cherts occur within the limestones. The upper part of the formation comprises marly shales and marls without cherts. Greenish grey colours dominate. The marls contain abundant traces of infauna. A few thin layers of black shales occur within this formation. 2. Czorsztyn

Castle (Czorsztyn

succession,

Figure

4).

This section is situated at the southern foot of the Czorsztyn Castle hill (Figure 1; Birkenmajer, 1963; Alexandrowicz, 1966, 1979) and is again in a trench. The Spisz Limestone, Chmielowa, Pomiedznik and lower part of the Jaworki Marl Formations are exposed. Only the cherts, considered by Birkenmajer (1977) to be typical of the lower part of the Pomiedznik Formation, are less numerous here than in the Falsztyn section. Thin layers of black shales also occur in this section.

Biostratigraphy

0 1

1

1

2

’

3

1

4

’

of the Pieniny

Klippen

221

Belt

5m

I

Figure 4. A. Czorsztyn Castle section, stratotype of the Czorsztyn succession according to Birkenmajer (1963, 1979), simplified. Czorsztyn succession: 1, Krempachy Marl Formation (Phensbachian-Aalenian); 2, Skrzypny Shale Formation (Aalenian-Bajocian); 3, Smolegowa Limestone Formation (Bajocian); 4, Krupisnka Limestone Formation (Bajocian-Bathonian); 5, Czorsztyn Limestone Formation (Callovian-Kimmeridgian); 6, Dursztyn Limestone Formation (Tithonian-Berriasian); 7, Lysa Limestone Formation (Berriasian-Valanginian); 8, Spisz Limestone Formation (Valanginian-Hauterivian); 9, Chmielowa Formation (Albian); 10, Pomiedznik Formation; 11, Jaworki Marl Formation, Grajcarek succession: 12. Szlachtowa Formation (Toarcian-Aatenian). B. Czorsztyn Castle trench. Ch, Chmielowa Formation; P, Pomiedznik Formation; MJ, Jaworki Marl Formation; Q, Quaternary; black sediments reflect anoxic events; numbers refer to location of samples.

I

I

0

1

1

8

2

1

3

1

4

1

Figure 5. Halka section, Czorsztyn succession (after Birkenmajer, 1963, 1979). SL, Smolegowa Limestone Formation, white crinoidal limestone (Bajocian); KL, Krupianka Limestone Formation, red crinoidal limestone (Bajocian-Bathonian); CL, Czorsztyn Limestone Formation, red nodular limestone (Callovian-Kimmeridgian); P, Pomiedznik Formation; MJ, Jaworki Marl Formation, green and variegated marls; black-sediments connected with anoxic events; numbers refer to location of samples.

.5m

1

XI. A. Gasiriski

222

3. Halka

(Czorsztyn

succession,

Figure

5).

‘l’his section is situated about one hundred metres to the southwest of the Czorsztyn Castle section, close to an abandoned bend of the Dunajec River (Figure 1; Birkenmajer, 1963; Alexandrowicz, 1966.) Part of it has been exposed in a trench. Rocks characteristic of the Chmielowa Formation are absent. Red nodular limestone (Callovian-Lower Kimmeridgian) of the Czorsztyn Limestone Formation is directly overlain by the higher part, as assessed by the absence of cherts (of the Falsztyn section) from the Pomiedznik Formation. The latter passes gradually upwards into green and variegated marls of the lower part of the Jaworki Marl Formation. A thin layer of black shale occurs within the Pomiedznik Formation. 4. KupuSnica

(Branisko

succession,

Figure

6).

This section is the type locality of the Kapubnica Formation. It is situated about one kilometre east of Niedzica Castle, on the opposite side of the Dunajec River, in a bluff by the road from Czorsztyn to Sromowce (cf. Birkenmajer, 1979, Figure 61). White and greyish cherty limestone of the Pieniny Limestone Formation (Tithonian-?Aptian) occurs at the base of the section in beds S-30 cm thick. This is overlain by the Rudina Member of the The lower, Brodno Member of the Kapusnica Kapusnica Formation. Formation is only rarely observed in the Polish part of the Pieniny Klippen Belt and is absent here. The Rudina Member comprises dark-grey, greyblue and green marly shales, with fine-grained sandstone intercalations, turbidites and a few layers of black shales. 5. Cisowiec (Branisko

succession,

Figure

6).

This section is exposed in a roadcut by the road from Krosnica to Katy (Figure l), about 500m from the top of Flaki Hill. The Pieniny Limestone

Figure

6.

KapuSnica

(tip)

and C~owec

(CIS) swtwns,

Branisko

succession.

PI, 1’1cnmy

Limestone

Formation, white cherty limestone (Tithonian-?Aptian); KP, Kapuinica Formation, upper partRudina Member; Q, Quaternary; black-sediments reflect anoxic events; numbers refer to location of samples.

Biostratigraphy

of the Pieniny

Klippen

and Kapusnica (Rudina Member) Formations are exposed exposure is small but relatively Iittle disturbed tectonically.

4. Taxonomic

223

Belt

here.

The

notes

Eighty-three species of foraminifers have been identified in about 300 samples. The distributions of the index species and the taxa having palaeoecological value are shown in Table 1. Discussions, with new opinions on the described species are presented below. Detailed morphological descriptions are omitted because these have been published before in Gasinski (1983) or are described elsewhere (e.g. in Robaszynski & Caron, 1979; Leckie, 1984; Weidich, 1984; Caron, 1985). Synonymies are given in many recent papers (e.g. Carter & Hart, 1977; Masters, 1977; Weidich, 1984). There is no need, therefore, to repeat these here. The dimensions of the studied specimens are within the range of variability of species described earlier (Gasinski, 1983), but morphological differences between the specimens are commented upon. Foraminiferal assemblages from Breggia were examined for comparison but were not analysed in detail. Classifications proposed by Loeblich & Tappan (1964, 1984), MagniezJannin (1975), Longoria (1974), Longoria & Gamper (1975), Masters (1977), Robaszynski & Caron (1979) and Caron (1985) are used. Most specimens were isolated from the rock matrix before being studied but some were examined in thin sections. The material is curated in Institute of Geological Sciences, Jagiellonian University (No. PKB-Micro, 86). For all dimensions given, t = thickness, D = diameter Family Globigerinelloididae Longoria, 1974 Subfamily Globigerinelloidinae Longoria, 1974 Genus Globigerinelloides Cushman & Ten Dam, 1948 Globigerinelloides bentonensis (Morrow, 1934) Figures 11 f-k

1934 Anomaha bentonensis Morrow, p. 201, pl. 30, figures 4a, b (catalogue of Ellis & Messina, 1940-l 975) Material: about 500 specimens Dimensions: D = 0.17-0.42 mm, t = 0.13-0.23 mm Remarks: Two species of Globigerinelloides, viz. G. bentonensis and G. caseyi (Bolli, Loeblich & Tappan), have been distinguished by the author (Gasinski, 1983) in the Pieniny material, mainly on the basis of the degree of test evolution. However, following Carter & Hart (1977), Leckie (1984), Caron (1985) and others G. caseyi is considered to be among the synonyms of G. ben tonensis . Specimens with somewhat evolute tests have been distinguished (Figures 11, j, k). The specimens selected from the sections of the Czorsztyn succession are bigger and more inflated than those from the sections of the Pieniny succession (D = 0.25-0.42 mm; Figure 11, k). Local stratigraphic range: Hedbergella assemblage to R. reicheli-R. greenhornensis Zones (Figure 7).

&owlec

I I

KapuSnlca section

Halka

action ___ .._.

Ic?r??!nI , 5ecI,on

,

Fa

Lsztvn

section

0 (7 K Samptes

Section

qaultina

(Morozova).

______~

-*

I

Biostratigraphy

of the Pieniny

Klippen

225

Belt

r

! i i

b

z

Assemblages

0 :

Proposed Local biozonation “I

505 lo?. 50% ldcn

t t

c

R.subticrensk- R.tiiinensls

1 c

d R.reicheli - R.qreenhornensi! ’ R.apwu%nica

i

P buxtorf!-R,apperrka

AE,

i

Figure

7.

Proposed

r

formal

local hiostratigraphic

Bbr~S

zonrs

PredlscosPha -era coiumnato

Erffellithus CC9 turriseiffelil

_ __Qsubt,cnenw~~a m

R tlclnensis

RDppemnca

R broken1

11977)

Mlcrorhabdu

1Slssmgh

-mep-Rre,c,,e,, “lo d,ik

-tocea

Rwshmonl

/

Mmantelll

\ 1

11985)

Caron

kcendyle umblicata

of the Alhian

-

--

Klippen

custunanl

P helvebca

Belt compared

I

Jb-i

in the Pieniny zones.

R gandolfr

archoeocretocea

and Cenomanian parastratigraphic

/Psubt,cmnenslsI

I -“Oides

Tglobotrunco -

W

nith

the latest

I

ortho-

zonatlon

proposed

-udy) rddltlonoi --.

and

1

7, -1

Biostratigraphr

of the

Pienin?;

Klippen

Belt

227

a

b ‘igure 8. Hrdbergella assemblage Zone. Microfacies with Hedbergella, x 60. a. Falsztyn section, upper part of the Chmielowa Formation: 1, Hedbergella delrioensis (Carsey); 2, above, juvenile form of Hedbergella planispira (Tappan); 3, left, Globigerinelhdes bentonensis (Morrou). b. Falsztyn section. uppermost part of the Chmlelowa Formation: 1, Hedbergella delrioensis (Carsey); 2, above, Hedbergella planispira (Tappan); 3, left, juvenile form of Globigerinelloides bentonensis (Morrow).

228

M. A. Gasiliski

b Figure 0. Hedbergella assemblage Zone. Mlcrofacies with Hedbergelfu, x 60. a. Falsztyn sectIon. 2, left. lowermost part of the Pomiedznik Formation: 1, above, Hedbergella planispira (Tappan); Hedbergella planispiva (Tappan); 3, right, Hedbergella delrioensis (Carsey), 4, right. Hedbergella planispira (Tappan); b. Czorsztyn Castle section, lowermost part of the Pomiedznik Formation: 1, Hedbergella delrioensis (Carsey).

Biostratigraphy

of the Pieniny

Klippen

Belt

229

b

e

ii

k m

t

n

Figure 10. Specimens selected from thin sections. a-d, Hedbergella delrioensis (Carsey), x 100, sample Fl-10; e.g. Praeglobotruncana aff. delrioensis (Plummer), x 80, FI-12; f, Rotalipora cf. appenninira (Renz), x 50, Fl-29; h. Tritaxia sp., x 50, Fl-14; i, Rotalipora cf. greenhornensis (Morrow), x 50, H8; j, PIanomaIina cf. buxtorfi (Gandolfi), x 50, k-3; k. ?Rotalipora sp., x60. (k-3; 1, Quinx 80, Kp-1; II, Lenticulina sp., queloculina sp., x 60, H-5, m, Rotalipora cf. subticinensis (Gandolfi) x 60. H-5.

230

IU. A. Gasiriski

Family Planomalinidae Bolli, Loeblich & Tappan, Genus Planomalina Loeblich & Tappan, 1946 Planomalina praebuxtorji Wonders, 1975 Figures 13e-h

1957

1975 Planomalina praebuxtorf Wonders, p. 90, pl. 1, figures la---c. Material: about 100 specimens Dimensions: D = 0.40-0.75 mm, t = 0.15-0.40 mm Remarks: The specimens are similar to those illustrated by Wonders (1975) from El Burrueco (Spain) and by Sigal (1979) from Leg 47 B, DSDP Site 398. Intermediate forms between ancestral G. bentonensis and P. buxtorji have been encountered. Many authors have followed Wonders (1975, 1980) and separated these intermediate forms as P. praebuxtorfi (Robaszynski & Caron, 1979; Leckie, 1984; Caron, 1985). It is used here as an index form and zonal marker (Figure 7). Local stratigraphic range: First Appearance Datum (FAD) and Last APwithin R. ticinensis- P. praebuxtorfi Zone (see pearance Datum (LAD) below). Planomalina buxtorji (Gandolfi, 1942) Figures 13i-1 1942 Planulina buxtorfi Gandolfi, p. 103, pl. 3, figure 7. Material: about 300 specimens Dimensions: D = 0.38-0.96 mm, t = 0.1 S-O.48 mm Remarks: Several morphological groups have been distinguished within P. buxtor$ according to morphological variations in the investigated material. Some of these are based on the development of the peripheral margin (more or less distinct), sutures (depressed to elevated) and the position and shape of the aperture. They may well represent separate taxa within this relatively long-ranging species (compare Figures 13i and 1). Similar features (i.e. the development and nature of the peripheral margin and the presence of less elevated sutures) were applied by Wonders for the erection of P. praebuxtor$ (1975). Most specimens from the Czorsztyn succession are larger (D =0.50-0.96 mm) and more involute than those from the so-called Trawne Beds (Gasinski, 1983) and are similar to those illustrated by Magniez- Jannin (1981) from Kent, UK. Ilocal stratigraphic range: R. ticinens&P. buxtorfi to P. buxtorj%R. appenninica Zones. Family Globotruncanidae Brotzen, 1942 Subfamily Hedbergellinae Loeblich & Tappan, 1961 Genus Hedbergella Bronnimann & Brown, 1958 Hedbergella delrioensis (Carsey, 1926) Figures 111-0, Figures 12a-i 1926 Globigerina cretacea d’orbigny var. delrioensis Carsey p. 43 (without illustrations in Longoria, 1974, pl. 54). Material: about 590 specimens Dimensions: D=0.20-0.60mm, t=O.lO-0.25 mm Remarks: H. infracretacea (Glaessner) has been previously (Gasinski, 1983) excluded from H. delrioensis because of its smaller size, lack of dominance of

x 130, sample Fl-1-I; b. c, Tritaxia gauftina FI@m 11. a, Glomospira rharoides (Jones and Parker). (Morozova), x 50, FL26; d. Dorothia oqrona (Rruss), x 60, u-3: e, Biticinclla breggiensis (Gandrllfi). x 100. Fl-4; f-k, Globigerinelloides bentonensi.~ (Morraw): f, g. x 100, N-16; h. i, x 150, Kp- 7; j. k. x 120. FI-10; ILo, Hedbrrgella delviovnsis (Came! 1. x I 50: I, lcp-4: In, 0, N-7; n, Cz-3.

232

>I. A. Gasitiski

the last chamber, and less spinose test. More recently, and as noted by Masters (1977), Leckie (1984) and C aron (1985), it is now considered to be a synonym of H. delrioensis, although others (Carter & Hart, 1977; Price, 1977a, b; Pflaumann & Krasheninnikov, 1977; Sigal, 1979; McNulty, 1979, 1984) still separate H. infracretacea. These authors have attached the rank of species to individual ecophenotypes without adequate analysis of the intraspecific variation (cf. Gasinski, 1983). Local stratigraphic range: Hedbergella assemblage to R. reicheli-R. greenhornesis Zones. Hedbergella planispira (Tappan, 1940) Figures 12j-1 1940 Globigerina planispira Tappan, p. 122, figures 12a-c (catalogue of Ellis & Messina, 1940-l 975) Material: about 300 specimens Dimensions: D = 0.13-0.26 mm, t = 0.06-0.13 mm Remarks: Differences in size of H. planispira have been connected with their stratigraphic range (Leckie, 1984), earlier forms being smaller, but these have not been observed in the specimens from the Hedbergella assemblage to R. uppenninica Zones. The specimens are similar to those illustrated by Robaszynski & Caron (1979) and described by Weidich (1984). Local stratigraphic range: Hedbergella assemblage to R. appenninica Zones. Hedbergella simplex (Morrow, 1934) Figure 12m; Figures 13a-d 1934 Hastigerinella simplex Morrow, p. 198, pl. 30, figure 6 (catalogue of Ellis & Messina, 1940-1975). Material: about 300 specimens Dimensions: D=0.18-O.SOmm, t=O.lO-0.18mm Remarks: H. amabilis (Loeblich & Tappan) and H. simplicissima (Magne & Sigal) are considered to be synonyms of H. simplex here (see also Robas1979 and Weidich, 1984). Leckie (1984) placed H. zynski & Caron, simplicissima in synonymy with H. amabilis, but he does not mention H. simplex. Weidich (1984) a 1so included H. jlandrini Porthault as a synonym of H. simplex, but these species have been considered distinct in many systematic studies (Robaszynski & Caron, 1979; Wonders, 1980; Caron, 1985). Several authors continue to use H. amabilis (Carter & Hart, 1977; Gradstein 1978; McNulty, 1979; Miles & Orr, 1980; Haig, 1981) and even H. simplicissimu (Masters, 1977; Peryt, 1980). Local stratigraphic range: R. ticinensis-P. buxtor$ to R. reicheli-R. greenhornenesis Zones. Subfamily Rotaliporinae Sigal, 1958 Genus Rotalipora Brotzen, 1942 Rotalipora appenninica (Renz, 1936) Figures 14h, i, k; Figures 15a-f 1936 Globotruncana appenninica Renz, p. 14, figure Messina, 1940-1975). Material: about 300 specimens Dimensions: D=0.38-0.65mm, t=0.16-0.32mm

2 (catalogue

Ellis

&

Biostratigraphy

Figure 12. a-i, Hedbergella Kp-7; j-l, Hedbergelh (Morrow). x 130, H-7.

delrioensis planispira

of the Pieniny

(Carsey):

(Tappan),

Klippen

x 100, sample x 150: j, Kp-0;

a-c,

Belt

233

d-f, x 120, Kp-4; g, I, x liU, k. 1. Fl-8; m, Hedbergella simpiex

Fl-14;

M. ‘4. (;asiriski

234

Figure

13.

.i\ -d. Hedbergella

Planomaha (Gandolfi):

simplex (Morrow): a, b. x 130, sample Kp-2; c, d, x 160. FL34; e-h, Wunders, x 80, e. h, I:l-14; f, G-1; 8. Kp-4; i I, Planomalina buxtoyfi i. x 80, Fl-29; j, x 60, Fl-22; k x 80. Cz-2; I, x 80. Kp-5. prnebuxtorfi

Biostratigraphy

of the Pieniny

Klippen

Belt

235

Remarks: Rotalipora balernaensis (Gandolfi) has been considered to be a synonym of R. appenninica by Wonders (1980), Gas&ski (1983) and Caron (1985) whereas Magniez-Jannin (1981; pl. 1, figure 4) distinguished both forms at subspecies level. Some authors have followed Wonders (1980) and suggested that R. gandol’ Luterbacher & Premoli Silva is a synonym of R. appenninica (e.g. Weidich, 1984). I n my opinion the difference between R. appenninica and R. gandolfi is not so great; both are probably ecophenotypes within the intra-specific variation of R. appenninica. However, in many recent papers R. gandoZ$ is distinguished as a separate species and is even used as a stratigraphic marker by Robaszynski & Caron (1979) and Caron (1985). I,ocal stratigraphic range: P. buxto+R. appenninica to the top of R. appenninica Zones. Rotalipora subticinensis (Gandolfi, 1957) Figures 14a-d 1957 Globotruncana ( Thalmanninella i ticinensis subsp. subticinensis Gandoll?, p. 59, pl. 8, figures la, c. Material: about 300 specimens Dimensions: D=0.28-O.SOmm, t=0.18-0.32mm Remarks: This species is not only of palaeobiological importance, being a form that is ancestral to R. ticinensis, but also of biostratigraphical value as a zonal marker (Robaszynski & Caron, 1979; Wonders, 1980; Caron, 1985). Nevertheless, some authors (e.g. Masters, 1977) include R. subticinensis in synonymy with R. ticinensis (Gandolfi). Local stratigraphic range: Hedbergella assemblage Zone (FAD unknown here) to the top of R. subticinensis-R. ticinensis Zone. Rotalipora ticinensis (Gandolfi, 1942) Figures 14e-g, j 1942 Globotruncana 10, 11.

tirinensis Gandolfi,

p. 113, pl. 2, figure 3; pl. 4, figures

Material: about 300 specimens Dimensions: D=0.35-0.65mm, t=0.18-0.32mm Remarks: The investigated specimens are similar to those from the type locality at Breggia. The palaeobiological significance of this species is also supported by suggestions of Caron (1985) that it should be included in the lineage T. praeticinensis-R. subticinensis--R. ticinensis. Specimens from the so-called Trawne Beds (Gasinski, 1983) and Kapusnica Formation are somewhat smaller (D=0.35-0.55 mm) than those from the Czorsztyn succession (D = 0.42-0.65 mm). Local stratigraphic range: Hedbergella assemblage Zone (FAD, unknown here) to the top of R. ticinensis-P. buxtorfi Zone. 5.

Biostratigraphy

The local biostratigraphic zones for the Albian and Cenomanian strata of the Pieniny Klippen Belt are based on the First and Last Appearance Datums (FAD and LAD respectively as above). They have been named according to the International Stratigraphic Guide (Hedberg, 1976) with some modifications and established in a similar way to those in Van Hinte

a-d, Rotalipora subticinensis (Gandolfi), x 80: a, d, sample Kp-1; b, FI-5; c, FI-4; e--g, j, ticinensis (Gandolfi), x 80: r---g, FILS: j. Kp-1; h, i, k. Rotalipora appenninica (Rrnz): i, k, x 80, F1-33; h, x 70, Kp-7.

Figure

14.

Rotaliporo

Figure 15. a-f, Rotolipora appenninica (Rem): a, b, x 100, sample Fl-33; 4; f, x 80, Kp-9; g, Pleurostomella reussi Berthelin, x 60, FI-27; h, (Berth&n), x 70, FL7; i, ?DentaZina sp., x 50, Fl-15; j-o, Radiolaria: koslouae k, Archaeodictyomitra sp., x 120, Fl-19; 1, o, Dictyomitra Praeoconoca~_vomma unitaersa Pessagno. x 160, FI-28: n. gen. indet.,

c, e, x 80, Cz-8; d, x 80, CisGavelinella ex. gr. intermedia j, Theocampe sp., x 80, Fl-28; Foreman, x 120, Kp-6; m, x 60, G-3.

(1976), Sigal (1977), Wonders (1980), Magniez-Jannin (1983), Leckie (1984), Weidich (1984). They are correlated with parastratigraphic and orthostratigraphic (ammonite) zones (see Figure 7) which have in turn been been established in stratotypic exposures and in many classical sections of the Albian-Cenomanian (Collignon et al., 1979; Robaszynski & Amedro, 1980; Amedro & Magniez-Jannin, 1981; MagniezzJannin, 1983). A second zonation scheme is also proposed (“Additional zonation” on Figure 7). This is aimed at facilitating practical application, i.e. the easier distinction of a biozone and rapid biostratigraphic diagnosis of a studied sample. It is based on local stratigraphic ranges of index taxa, and the zones are Taxon Range Zones (TRZs). For example, R. ticinensis may be used as a TRZ within the R. ticinensis-P. praebuxtorfi Local Concurrent Range Zone (LCRZ) and R. ticinensis-P. buxtorji Local Partial Concurrent Range Zone (LPCRZ). P. buxtorfi may be used as TRZ within R. tic&ens&P. buxtor$ LPCRZ and P. buxto+R. appenninica LCRZ. 5.1.

Hedbergella

local assemblage

zone (LAZ,

informal)

‘l’he zone is distinguished in the upper part of the Chmielowa Formation and the lowermost part of the Pomiedznik Formation only in the Czorsztyn succession. Besides being dominated by Hedbergella (H. delvioensis and H. planispira; Figures 8, 9), the assemblages include several specimens of G. bentonensis (Morrow), B. breggiensis (Gandolfi), rare Ticinella sp., occasional specimens of agglutinated taxa (Tritaxia sp., Dorothia sp.) and miliolids (Quinqueloculina sp.; Figures 10, 11). ‘I’hey also contain small numbers of Nodosariacea. Similar assemblages have been described by Alexandrowicz (1966) in the “Hedbergella microfacies” which he distinguished in the Chmielowa Formation. The foraminiferal assemblages and the succession of strata indicate that the zone is older than late Albian. It is situated lower in the sequence than the R. subticinensis-R. ticinensis Zone defined below. The occurrence of B. breggiensis (cf. Caron, 1985) and the absence of Rotalipora suggest a middle Albian age. A. subticinensis may occur (FAD) in the upper part of this zone, but its presence could not be ascertained because the assemblages in the hard limestones of this part of the section could be studied only in thin sections. 5.2. Rotalipora subticinensis-Rotalipora ticinensis LCRZ Lower boundary: top of Hedbergella assemblage Zone (with unknown FAD of R. subticinensis) Upper boundary: FAD of P. praebuxtorji and LAD of R. subticinensis Remarks: The zone established here is used in a narrower sense than by Robaszynski & Caron (1979). Many authors have used R. subticinensis and R. ticinensis as the index species for the separation of interval zones (Wonders, 1980; Caron, 1985). R. subticinensis and R. ticinensis Subzones within the B. breggiensis Zone have been established by Leckie (1984; see also Figure 7). Planktonic foraminifers constitute about 809:, of the whole assemblage (index taxa S-200/“). Hedbergella dominates (Table 1). Agglutinated foraminifers are most numerous in the Kapusnica section (Table 1) where their occurrence coincides with the beginning of the turbidite sequence within the Pieniny-Branisko succession.

Biostratigraphy

of the Pieniny

Klippen

Belt

239

5.3. Rotalipora ticinensis-Planomalina praebuxtorji LCRZ Lower boundary: FAD of P. praebuxtorfi and LAD of R. subticinensis Upper boundary: FAD of P. buxtorji and LAD of P. praebuxtorfi Remarks: This zone and the next two are included here in the Vraconian stage (Figure 7) which, according to Harland et al. (1982), was distinguished by Renevier in 1867 within the Stoliczkaia dispar Zone. Many authors (e.g. Price, 1976; Van Hinte, 1976; McXulty, 1979; Pflaumann & Krasheninnikov, 1977; Premoli Silva et al., 1977; Haig, 1981; Arthur & Premoli Silva, 1982) use the name Vraconian for latest Albian strata but some, including Harland et al. (1982), do not accept it. A detailed subdivision of the interval with P. buxtorji was made possible by the erection of P. praebuxtorji (Wonders, 1975) and the subsequent distinction of the P. praebuxtor$ Zone (Wonders, 1980). The P. praebuxtoyfi and P. buxtorJi zones as proposed here are also TRZs within the additional zonation scheme (Figure 7). The species P. praebuxtorji and the corresponding zone have been not distinguished in the author’s earlier papers (Gasinski, 1983, 1984). Leckie (I 984) has distinguished the P. praebuxtorji Subzone within the P. praebuxtor$--P. buxtorji Zone (Figure 7). Hedbergella dominates the assemblage as for the preceding zone, and agglutinated foraminifers increase gradually in number upwards within the turbidite facies of the Kapusnica Formation (Table 1). Both the index species and G. bentonensis constitute up to about loo,, of the whole assemblage. 5.4. Rotalipora ticinensis-Planomalina huxtor$ I,PCRZ (cf. Van Hinte, 1976) 1,ower boundary: FAD of P. buxtor$ and LAD of P. praebuxtorfi Upper boundary: FAD of R. appenninica Remarks: R. subticinensis and R. ticinensis zones are proposed in my second scheme (Figure 7) as TRZs. The definition of the R. ticinensis-P. buxtorfi Zone differs from that of Wonders (1980; from FAD of P. buxtorji to LAD of P. ticinensis) and also from my earlier scheme (in Gas&ski, 1983); because the stratigraphical range of R. appenninica (Renz) has been revised and P. praebuxtorfi separated from P. buxtorfi. Specimens of Hedbergella and Rotalipora dominate in the planktonic assemblage (Table l), although the former is not as abundant as in the previous zones. The percentage of agglutinated taxa is greater than in the R. ticinensis-P. praebuxtorji LCRZ. 5.5.

Planomalina

buxto+Rotalipora

appenninica

LCRZ

1,ower boundary: FAD of R. appenninica Upper boundary: LAD of R. ticinensis and LAD of P. buxtorfi Remarks: This zone as used here differs from the T. appenninica-P. buxtorji Zone of Wonders (1980; from LAD of P. ticinensis to LAD of P. buxtorfi). The foraminiferal assemblage is more diverse and has a greater proportion of agglutinated taxa than that of the preceding zone (Table I). 5.6.

Rotalipora

appenninica

LPRZ

Lower boundary: LAD of P. buxtorfi and LAD of R. ticinensis Upper boundary: FAD of R. reicheli and FAD of R. greenhornensis Remarks: The R. appenninica Zone is designated an interval zone (IZ)

by

XI. t\. Gasiriski

240

Robaszynski & Caron (1979), Wonders (1980), Leckie (1984) and Caron (1985). It is proposed here as a TRZ in the second zonation scheme (Figure 7). It has not been distinguished in the Falsztyn section because the beds concerned are not exposed. Agglutinated taxa are more numerous than in the preceding zone, especially at the horizon represented by sample Kp-9 (Table 1). 5.7.

Rotalipora

reicheli-Rotalipora

greenhornensis

LPCRZ

Lower boundary: FAD of R. reicheli and FAD of R. greenhornensis. Upper boundary: FAD of R. cushmani (in overlying sediments-see Gasinski, 1983). Remarks: Some authors (e.g. Robaszynski & Caron, 1979; Caron, 1985) deny the coexistence of R. reicheli with R. greenhornensis but both forms are concurrent in the Pieniny Klippen Belt (Gasinski, 1983; this paper), in Breggia (southern Alps) and Moria (Umbria-Marche Apennines; personal observations). This zone has been found here only in the Halka section. The benthonic component consists exclusively of agglutinated taxa in some samples (H-7, H-8; Table 1). 6.

Palaeoecological

conclusions

The studied material reveals no evidence of reworking according to the criteria of McNulty, (1984; broken, worn and etched specimens). The assemblages are dominated by planktonic species which belong mainly to Planomalina, Hedbergella and Rotalipora. A similar Globigerinelloides, dominance was also noted by Butt (1981) from the CampanianMaastrichtian of the eastern Alps. A high percentage of agglutinated foraminifers (up to 100 per cent; sample Kp-9) was found to be present in some samples, especially those collected from turbidites. Although their numbers increase with increasing frequency of turbidite intercalations they only rarely attain values as high as in the “Trawne” Beds (see Gasinski, 1983, Figures 5,6). They also occur in low diversity assemblages mainly composed of Ammodiscus, Dorothia, Glomospira, Tritaxia, Spiroplectinata and Arenobulimina. The calcareous benthic assemblages encountered consist mainly of Pleurostomella, Osangularia, Gyroidinoides and Gavelinella. Nodosariacea (mainly Lenticulina spp., Tribrachia excavata (Reuss), Nodosaria spp.) are the only calcareous benthic foraminifers of palaeoecological significance. They are more numerous in the shallow facies of the Czorsztyn succession, especially in the Czorsztyn Castle section (Table l), than in the Alexandrowicz (1979) similarly recorded a Pieniny-Branisko sequence. large proportion of Nodosariacea in the Czorsztyn succession. Assemblages with a higher content of Nodosariacea that reflect deposition in relatively shallow environments have also been observed by Sliter, (1972, 1977), Scheibnerova, (1976), Olsson, (1977), Haig, (1979 a, b, 1981) and Butt, (1981). These belong to the upper part of the “Marssonella” association of Haig (1979a). ‘I’he planktonic forms are of little help for determining palaeobathymetry. Hedbergella is epipelagic and becomes more numerous with increasing

Biostratigraphy

of the Pieniny Klippen Belt

241

distance from shore (Sliter, 1972; Sliter & Baker, 1972; Olsson, 1977; Scheibnerova, 1976 and others). The presence of Rotalipora does, however indicate the bathypelagic realm (Sliter, 1972). Three palaeobathymetric associations have, therefore, been established: in which the assemblages contain a 1. The “Czorsztyn association” moderate number of nodosarids and a mixture of miliolids including rare specimens of Quinqueloculina sp.; agglutinated taxa are relatively rare except in the uppermost part of the Halka section. It corresponds to the upper part of the “Marssonella” association referred to above. which consists of assemblages that are 2. The “Pieniny A association” dominantly planktonic and contain only a few nodosarids. It suggests deposition in approximately the middle part of the slope. in which the assemblages are similar to 3. The “Pieniny B association” those of the previous association and represent a similar depth range, but It is characteristic of pelagic have a greater agglutinated component. sediments which include numerous turbidite intercalations. The associations described earlier from the “Trawne” Beds (Gasinski, 1983) probably belong to this group. All of these associations are of only local significance. They permit the differentiation of palaeobathymetric zones solely within the sedimentary basin of the Pieniny Klippen Belt. They also changed with time. During the Late Cretaceous the deposition of turbidites extended northwards, covering almost the whole area of the Pieniny Klippen Belt basin. Consequently nearly all the Late Cretaceous foraminiferal associations in this basin are of the “Pieniny B” type. Somewhat similar criteria as above have been used by Slaczka & Gasinski (1985) for defining “A”, “B” and “C” associations in the Senonian of the Silesian unit of the Outer Carpathians. It is evident from Table 1 that some samples directly overlying black shales, which are interpreted as the record of episodes of bottom water anoxia, are enriched in radiolarian assemblages. This may be explained by overturn and upwelling of nutrients that accumulated in bottom waters during the anoxic events (cf. Schlanger & Jenkyns, 1976; Arthur & Schlanger, 1979; Diester Haass & Schrader, 1979; Arthur & Premoli Silva, 1982; Bralower & Thierstein, 1984). Rare inoceramid prisms and fish teeth (Table 1) have limited significance. The former probably indicate redeposition by turbidity currents from shallower environments. 7. Comparison Apennines

with

the

southern

Alps

and

Umbria-Marche

Assemblages from Breggia (Lombardy Basin of the southern Alps, Ticino, Switzerland; Gandolfi, 1942; Schaub & Luterbacher, 1965) and from the Moria section in the Umbria-Marche Apennines (cf. Wonders, 1978, 1980; de Boer, 1982; Habib, 1982; Schlanger & Cita, 1982) have been compared with those from the Pieniny Klippen Belt. The lithostratigraphy of the Breggia section is shown in Figure 16, together with the proposed biostratigraphic correlation with the Pieniny Klippen Belt. It is the type locality for several species of planktonic foraminifers (Gandolfi, 1942). The contents of washed material from several samples taken from this section are considered

here. ‘I‘he assemblages are better preserved than those from the Pieniny Klippen Belt but are similar in composition. In my opinion the assemblages from the Breggia section belongs to the “Marssonella” association of Haig (1979 a) and presumably reflect deposition in a middle slope environment. The Moria section in the Marche-Umbria area has been recently investigated by Coccioni & Gasinski (in preparation). It is the type area for several species and subspecies of planktonic foraminifers (Renz, 1936). Coccioni & Gasinski propose a biostratigraphical scheme which modifies and is more detailed than that established earlier by Wonders (1978, 1980), and corresponds with that proposed here for the Pieniny Klippen Belt (Figure 16). ‘l’he assemblages are more similar to those from the belt than those from Breggia. I have also collected samples from well-known Gubbio-Bottaccione section (Umbria-Marche, see Pialli, 1977; Premoli Silva, 1977) but these contain only poor and badly preserved assemblages of planktonic foraminifers. Since the samples could be studied only in thin section because of the hardness of the cherty limestones, closer comparison with the material from the Pieniny Klippen Belt was precluded.

Breggia

II -R. qeenhornensi

xtwfl -R appenninica .ticinensis-Plzuxtarfi ems- Ppraebuxto

Figure 16. Local biozones established in the Pieniny Klippen Belt compared with those distinguished within the Breggia section of the southern Alps, Lombardy Basin, Ticino, Switzerland (cf. Gandolfi, 1942; Schaub & Lauterbacher, 1965, simplified) and with the M&a section of UmbriaMarche Apennines (Cocci& & Gasiriski, in preparation, simplified). 1, limestones (Maiolica, Biancone); 2, cherts; 3, marly limestones, marlstones, marly shales; 4, black shales.

Biostratigraphy

8.

of the Pieniny Klippen Belt

243

Cretaceous Oceanic Anoxic Events in the Pieniny Klippen Belt

The layers of black shales intercalated within the Albian and Cenomanian strata of the Pieniny Klippen Belt may be attributed to the Cretaceous oceanic anoxic events that have received so much attention following their recognition and correlation in Deep Sea Drilling material and in many areas on land (cf. Schlanger & Jenkyns, 1976; Schlanger & Cita, 1982; Bralower & Thierstein, 1984; Reyment & Bengtson, 1986). Although they have been not studied in detail, their correlation with other occurrences is attempted here. Three local anoxic events (AEs) are suggested equivalents of Oceanic Anoxic

Event

1 (OAE

1, Barremian-Albian

of Arthur

& Schlanger,

1979).

AE-1 occurs within the R. subticinensis-R. ticinensis LCRZ (samples: Kp-0, Fl-9), AE-2 is within the R. ticinensis-P. buxtorfi LCRZ (samples: Cz-3, Fl19) and AE-3 is within the P. buxtor$-R. appenninica LCRZ (samples: H-4. Cz-6, Fl-34). Sediments that were deposited in anoxic conditions occur in similar positions in the Moria (Coccioni & Gas&ski, in preparation) and Breggia sections (Figure 16; “scisti bituminosi” of Gandolfi, 1942, pl. 1). The Cenomanian-Turonian OAE 2 of Arthur & Schlanger (1979), also known as “Live110 Bonarelli”, occurs in the Pieniny Klippen Belt. It is suggested by both Birkenmajer & Jednorowska’s (1984, r in Figure 3) lithological description and the stratigraphical position of the Magierowa Skalka section. The black shales in the belt, as well as in the Breggia and Moria sections are interstratified with other pelagic deposits. This suggests that anoxic conditions occurred rhythmically (Reyment Sz Bengtson, 1986, p. 42). The foraminiferal assemblages are different in the deposits attributed to different anoxic events. Samples H-4 (AE-3) and Fl-19 (AE-2) in the Czorsztyn succession comprise mainly planktonic assemblages without calcareous benthos. This suggests anoxia in bottom waters (model A of Arthur & Schlanger, 1979; a restricted basin with stratified water and anoxia in the lower layer as in the modern Black Sea). By contrast, calcareous benthos is present in samples Fl-9, Kp-0 (AE-I), Cz-3 (AE-2), Fl-34 and Cz-6 (AE-3). The strata from which these assemblages come may be interpreted to represent conditions of mid-water oxygen minimum (model B of Arthur & Schlanger, 1979).

Acknowledgments I wish to express my

gratitude to Professor S. Geroch (Jagiellonian University) and Professor K. Birkenmajer (Polish Academy of Sciences) for their suggestions given during the course of this study. Professor Birkenmajer introduced me to the geology of the area investigated. Sincere thanks are also extended to Professor A. Slgczka, Dr. E. Porebska (Jagiellonian University), Dr. G. Haczewski (Polish Academy of Sciences) and the late Docent W. A. Nowak (Geological Institute of Krak6w) for their valuable discussions as well as to Docent H. G&-ka (Warsaw Univeristy) for

244

M.

A. Gasiriski

assistance in identifying radiolarians. Special thanks go to Professor F. Proto Decima (University of Padua), Dr. R. Coccioni (University of Urbino) and to other Italian friends for their hospitality during my stay in Italy. The material from Breggia was collected by Prof. Proto Decima during the field excursion of the 9th European Micropalaeontological Colloquium and was generously given to the author. All scanning electron micrographs were obtained using a JEOL JSM-3.5 SEM in the Laboratory of Electron Microscopy of the Zoological Institute of Jagiellonian University. Part of this study was supported by a Jagiellonian University Postdoctoral Fellowship. References Alexandrowicz, S. W. 1966. La stratigraphie du Cretace superieur et moyen dam la partie polonaise de la zone des Klippes Pieninnes. Zeszyty Naukowe Akademii Gdmiczo-Hutniczej, Geologia. Rozprawy 78, 1-142. [In Polish, French abstract] Alexandrowicz, S. W. 1979. Albian Foraminifera of the Czorsztyn Series, Chmielowa Formation of the Pieniny Klippen Belt. Annales de la SocittC Ggologique de Pologne 49, 1655183. [In Polish, English abstract] Alexandrowicz, S. W. Birkenmajer, K. & Geroch, S. 1962. Microfauna and age of brick-red Globotruncana marls (Puchov Marls) of the Pieniny Klippen Belt of Poland. Bulletin de I’Academie Polonaise

des Sciences 10,91-98. Alexandrowicz, Cretaceous

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Collignon, M., Sigal, J, & Grekoff, N. 1979. (Madagascar) et ses faunes d’ammonites,

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Pieniny

Klippen

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