S T U D I A G E O L O G I C A P O L O N I C AVol. 124, Kraków 2005, pp. 259–272.

Methods and Applications in MicropalaeontologyEdited by J. Tyszka, M. Oliwkiewicz-Miklasiñska,

P. Gedl & M. A. Kaminski

Anna LEMAÑSKA1

Comparison of deep-water agglutinated foraminifera

from the hemipelagic variegated shales

(Lower Turonian–Lower Santonian) and the turbiditic

Godula beds (Upper Santonian–Campanian)

in the Lanckorona-Wadowice area (Silesian Unit,

Outer Carpathians, Poland)

(Figs 1–7)

Abstract. Deep-water agglutinated foraminifera (DWAF) have been studied from variegated shalesand Godula beds exposed in the vicinity of Kalwaria Zebrzydowska (Silesian Nappe, Outer Carpa-thians, Poland). Following the standard foraminiferal zonation scheme of Geroch & Nowak (1984),the studied variegated shales can be correlated with the Uvigerinammina jankoi Zone (LowerTuronian–Lower Santonian). The Godula beds can be correlated to the Caudammina gigantea Zone(Upper Santonian–Campanian). Foraminiferal assemblages from the variegated shales are dominatedby infaunal and semi-infaunal forms. Their occurrence suggests aerobic bottom water conditionsassociated with low organic matter availability during the deposition of this unit. Such conditions arepresumably related to slow sedimentation rate in low energy, well-oxygenated and oligotrophicbottom environment. In contrast, foraminiferal assemblages from the Godula beds are dominated byepifaunal forms, which collected food from the sediment/water interface. It may suggest thatsedimentation took place under relatively higher energy conditions with a higher organic matter flux.

Key words: biostratigraphy, palaeoecology, agglutinated foraminifera, morphogroup analysis,variegated shales, turbidities, Carpathians.

INTRODUCTION

The variegated shales and the Godula beds were deposited in the Silesian basinin deep-water conditions below the CCD. The sedimentation of the variegated

1 Jagiellonian University, Institute of Geological Sciences, Oleandry 2a, 30-063 Kraków, Poland.E-mail: leman@ing.uj.edu.pl

shales began during the Early Turonian. These sediments consist of red shales withsubordinate green shale intercalations. Thin-bedded very fine-grained glauconiticsandstones occur infrequently in this lithostratigraphic unit. The variegated shalesare interpreted as deep-sea hemipelagic sediments deposited by the settling of indi-vidual grain particles resedimented from proximal areas by bottom currents and/orfrom highly dispersed turbiditic currents (Leszczyñski & Uchman, 1991). The Go-dula beds consist of turbiditic glauconitic sandstones interlayered with grey-greenish shales and, in the upper part, by red shales. This lithostratigraphic unitoverlies the Barnasiówka Radiolarian Shale Formation or the variegated shales andunderlies the Istebna sandstones. Sedimentation of the Godula beds took placewithin a shifting system of submarine fans (S³omka, 1995). The thickness of thesesediments decrease eastwards where hemipelagic sedimentation prevail over tur-biditic one. This is recorded by the alternation of the thick-bedded facies of the Go-dula beds with the hemipelagic facies of the variegated shales.

This paper compares of deep-water agglutinated foraminifera from the varie-gated shales and the Godula beds of the Silesian succession exposed in theLanckorona-Wadowice area (Outer Carpathians). The aim of the present study isreconstruction of bottom water conditions during sedimentation of these two differ-ent facies.

GEOLOGICAL SETTING

The Silesian Nappe east of the Skawa dislocation divides in two variously devel-oped parts separated by the Lanckorona tectonic zone: the northern one consistingof Upper Cretaceous strata and the southern part consisting mainly of Oligoceneand Lower Miocene Krosno beds (Ksi¹¿kiewicz, 1951, 1977). The Lanckorona-Wadowice area is situated in the northern zone. The Upper Cretaceous sediments ofthis area consist of the upper part of the Lgota beds, the Barnasiówka RadiolarianShale Formation, the variegated shales, the Godula beds and the Istebna sandstones(Fig. 1).

The oldest sediments, the upper part of the Barnasiówka Radiolarian Shale For-mation (see B¹k et al., 2001), consists of thin-bedded glauconitic siliceous sand-stones and light-greenish and green non-calcareous shales with pseudomorphs aftercarbonates such rodochrosite (Wieser, 1985). This lithostratigraphic unit is over-lain by the variegated shales consisting of brick-reddish claystones and a subordi-nate series of green non-calcareous shales, intercalated with thin black manganifer-ous shales (tuffites?), very thin layers of light-green bentonite and thin-beddedglauconitic sandstones. The Godula beds are characterized by a higher number ofglauconitic sandstones and mainly greenish-grey colour of mudstones. Infrequentintercalations of thin red shales occur in the upper part of the Godula beds. Thethickness of the variegated shales in the study area is about 150–250 meters(Ksi¹¿kiewicz, 1951) and that of the Godula beds reaches from 200 to 600 meters(S³omka, 1995). The youngest deposits exposed in this area are the Istebnasandstones.

260 A. LEMAÑSKA

MATERIAL AND METHODS

The studied section crops out in a small creek and its tributary at KlasztornaGóra hill south of Kalwaria Zebrzydowska (Figs 1, 2). The upper part of the Barna-siówka Radiolarian Shale Formation, the variegated shales, the Godula beds andthe lower part of the Istebna sandstones are exposed there. Thirty samples havebeen collected from red and green shales of the variegated shales and with upper-most turbiditic sequences and grey-greenish and red shales of the Godula beds.Their position is shown in Fig. 3. Samples about 0.5 kg each have been processedthe following standard method based on solution of Glauber’s salt, warming/freez-ing cycles and final washing through sieves with a 63 µm mesh diameter.

A total of 300 specimens of foraminifera have been picked out from each sampleand mounted on cardboard microscope slides. For morphogroup analysis of frag-ments of tubular species and multi-chambered, uniserial forms (Reophax, Caudam-

mina) were counted individually and then their number was recalculated taking intoaccount dimensions of unchanged forms (B¹k, 2004).

Scanning electron microscope photomicrographs have been taken in the Labo-ratory of Field Emission Scanning Electron Microscopy and Microanalysis in theInstitute of Geological Sciences of the Jagiellonian University.

RESULTS

The studied samples contain deep-water agglutinated foraminifera (Figs 4, 5).Two qualitatively and quantitatively different assemblages have been found. The

CRETACEOUS DEEP-WATER AGGLUTINATED FORAMINIFERA 261

Fig. 1. Tectonic map of the of the Silesian Unit at the studied section (after Ksi¹¿kiewicz, 1977)

one from the variegated shales consists of long-ranging fine-grained small dimen-sion species representing the following genera: Rhabdammina, Hyperammina,Rhizammina, Glomospira, Ammodiscus, Trochammina, and Recurvoides. Uvigeri-

nammina and Gerochammina occur there as well (see in details in Fig. 4). Unidenti-fied specimens of radiolarians and sponge spicules have been found in the investi-gated variegated shales.

The foraminiferal assemblage from the Godula Beds is composed mainly ofcoarse-grained large-sized forms: Rhabdammina, Nothia, Psammosphaera, Reo-

phax. Additionally Caudammina gigantea (Geroch) and Caudammina ovulum

(Grzybowski) occur frequently. Single specimens of Hormosina crassa (Geroch)have been observed too. Other forms like Bathysiphon, Ammodiscus, Glomospira,Trochammina, Trochamminoides, and Paratrochamminoides are less frequent.

BIOSTRATIGRAPHY

Interpretation

Following the standard foraminiferal zonation scheme of Geroch & Nowak(1984), the studied variegated shales can be correlated with the Uvigerinammina

jankoi Zone. The Godula beds can be correlated to the Caudammina gigantea Zone.The age of the younger foraminiferal assemblage with Caudammina gigantea

262 A. LEMAÑSKA

Fig. 2. Geological map of the studied section with indicated samples location at KalwariaZebrzydowska (after Szymakowska & ¯ytko, 1965): Kw – Verovice shales; Kl1 – lower Lgota beds;Kl2 – middle Lgota Beds; Kl3 – Mikuszowice cherts; Kps

m – marls; Kbr – Barnasiówka RadiolarianShale Formation; Kps – variegated shales; Kg2 – middle Godula beds; Ki – Istebna beds; Olk – Krosnobeds

(Geroch) can be estimated as the Late Santonian–Campanian. This is based on theco-occurrence of the index species, which is known to appear throughout the LateSantonian–Early Campanian (Olszewska, 1997) and Hormosina crassa (Geroch),the stratigraphic range of which is Barremian–Cenomanian (Geroch & Nowak,1984), respectively up to the Early Senonian according to Morgiel & Olszewska(1981). However, some authors report the occurrence of Caudammina gigantea

(Geroch) from younger strata, i.e., Lower Campanian–Maastrichtian (Geroch &Nowak, 1984).

The precise dating of the first appearance of Caudammina gigantea (Geroch) isimportant for the age-assessment of the top of older Uvigerinammina jankoi Zone.

CRETACEOUS DEEP-WATER AGGLUTINATED FORAMINIFERA 263

Fig. 3. Lithostratigraphical column of the studied sediments, Silesian Unit (after Lemañska &Gedl, submit., modified)

264 A. LEMAÑSKA

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CRETACEOUS DEEP-WATER AGGLUTINATED FORAMINIFERA 265

Fig. 5. Microfauna from variegated shales and Godula beds. 1 – Rhabdammina sp., Pg-3/03; 2 –Nothia sp. – Kz-7/03; 3 – Bathysiphon microrhaphidus (Samuel) – Kz-8/03; 4 – Hyperammina

elongata (Brady), Kz-8/03; 5 – Kalamopsis grzybowskii (Dyl¹¿anka) – Pg-3/03; 6 – Hormosina

velascoensis (Cushman) – Pg-3/03; 7, 8 – Hormosina crassa (Geroch) – Kz-10/03; Pg- 2/03; 9, 10 –Caudammina gigantea (Geroch) – Kz-1/03, Kz-6/03; 11 – Reophax duplex (Grzybowski), Kz-6/03;12 – Psammosphaera fusca (Schultze) – Kz-7/03; 13 – Ammodiscus cretaceous (Reuss) – Kz-10/03;14 – Rzehakina minima (Cushman & Renz) – Kz-6/03; 15 – Paratrochamminoides olszewskii

(Grzybowski), Kz-10/03; 16 – Trochammina globigeriniformis (Jones & Parker) – Kz-10/03; 17 –Rhizammina sp. – Pg-3/04; 18 – Gerochammina sp., Pg-5/03; 19 – Uvigerinammina jankoi (Majzon),Pg-3/04; 20 – U. jankoi (Majzon) – Pg-8/03; 21 – Haplophragmoides mjatliukae (Maslakova) –Pg-8/03; 22 – Recurvoides sp., Pg-9/03; 23 – Radiolaria – Pg-5/03; 24 – Radiolaria – Pg-9/03; 25 –Sponge spicule – Pg-5/03; 26 – Sponge spicule – Pg-9/03; 27 – Sponge spicule – Pg-5/03; scale bar100 µm

Its base can be estimated as not older than the Early Turonian because the first ap-pearance of Uvigerinammina jankoi (Majzon) is known from this period (Geroch,1957; Geroch & Nowak, 1984; Kuhnt, 1992; B¹k, 1998). Thus, the age of the lowerpart of the variegated shales in the studied section is Lower Turonian–Lower Santo-nian, whereas the age of overlying Godula beds is the Upper Santonian– Cam-panian.

Discussion of biostratigraphy

The age of the variegated shales and the Godula beds have been studied earlier.For the first time the age of the Godula Beds was described by Hohenegger (1861)as Albian on the base of Desmoceras dupinianum (d’Orb.). The same age of thevariegated shales has been estimated as Albian on the basis of species of Ticinella

(Hanzlíková et al., 1954; see Fig. 6).Contemporary investigations prove that the age of the lower part of the varie-

gated shales is estimated as Lower Turonian (B¹k et al., 2001). The age of the Go-dula beds was described by B. Olszewska (in S³omka, 1995). The lower part of theGodula beds is not older than Turonian and is clearly diachronic in different parts ofthe Outer Carpathian. At the studied section the age of the Godula beds is estimatedas Upper Santonian–Campanian. It could indicate that the sedimentation of the Go-dula beds began during the late Early Senonian. It is relevant with development ofthe variegated shales at this area.

PALAEOECOLOGY

Morphogroups

Fossil deep-water agglutinated foraminifera can be used as a tool for reconstruc-tion of sedimentary environments and documenting palaeoceanographic changesin the past. Their palaeoecological habitats are interpreted from comparison withmorphologically similar recent living forms, which mode of live is well known.Taking into account shape of test and chamber arrangement, five morphogroupscharacterizing various life strategies have been distinguished (Corliss, 1985; Jones& Charnock, 1985; Kaiho, 1991; Nagy, 1992; Tyszka, 1994; Nagy et al., 1995; Ka-minski et al., 1995; Kuhnt et al., 1996; B¹k et al., 1997, B¹k, 2004).

Morphogroup A1 comprises tubular, branched forms like Bathysiphon,Rhabdammina, Hyperammina, and Rhizammina. Nothia have been classified in tothis morphogroup but their feeding strategy is not clear. Other authors classifiedthis forms to morphogroup A2 (i.e., Geroch & Kaminski, 1992). These forms aresuspension feeders, which tend to live as erect epifauna, building a pseudopodialnet above the sediment/water interface in order to reach food. Frequent occurrenceof suspension feeders in sediment reflects moderate to low levels of organic flux tothe sea bottom and their size may be used to estimate changes in palaeoproductivity(Kaminski & Kuhnt, 1995; Gasiñski, 1998). The number of specimens and size oftheir tests increases with higher flux of organic matter to the bottom.

266 A. LEMAÑSKA

Morphogroup A2 consists of flattened, planispiral coiled and irregular formssuch as Ammodiscus, Glomospira, Trochamminoides, Paratrochamminoides andRzehakina.

Foraminifera representing this morphogroup have various feeding strategy.Some forms like modern Ammodiscus are mobile epifaunal detritivores (Nagy et

al., 1995), some living species of Glomospira live at the surface of the sediment orwithin its topmost 1.5 cm (Mackensen & Douglas, 1989). The forms belonging tothis morphogroup characterize higher energy environments also with increased in-fluence of turbidity currents (Kaminski & Kuhnt, 1989).

Morphogroup A3 comprises plano-convex and concavo-convex forms such asTrochammina, Saccammina and Psammosphaera. They live at the bottom surfacewith the aperture directed into sediment (Nagy et al., 1995). They also can attach toinvertebrate shells (Mackensen & Douglas, 1989) or tube forms like Rhabdammina

(Nagy et al., 1995). These forms live as epifaunal detritivores and herbivores.

CRETACEOUS DEEP-WATER AGGLUTINATED FORAMINIFERA 267

Fig. 6. Stratigraphically important fossils from the variegated shales and the Godula beds inSilesian Nappe (Outer Carpathians)

Morphogroup A4 includes rounded forms like Recurvoides and Haplophrag-

moides. They are detritivores and live as shallow infauna, 1–4 cm below the sedi-ment surface.

Morphogroup A5 consists of elongated subcylindrical or tapered forms: Kar-

rerulina, Gerochammina, Spiroplectammina, Hormosina, Uvigerinammina, andReophax. They all are detritivores and could be found even more than 10 cm belowthe sediment surface like Recent Reophax (Kaminski et al., 1988; Hunt & Corliss,1993; Mackensen & Douglas, 1989). The forms with this feeding strategy occur inwell-oxygenated, oligotrophic waters. But on the other hand, they may also occurunder strongly dysoxic conditions where anaerobic degradation of organic mattermay provide an additional food source around the redox front (Jorissen et al., 1995).

The proportions of agglutinated foraminiferal morphogroups are related to theenvironmental conditions prevailing in the bottom waters and within the topmostpart of the sediment. Changes of these proportions may reflect changes in organicflux into bottom (Gooday, 1988, 1994), bottom water oxygenation (Kaiho, 1994;Kaminski et al., 1995) and the energy of bottom currents (Schröder et al., 1988;Kuhnt et al., 2000).

Interpretation of environmental conditions

The foraminiferal assemblage from the variegated shales is dominated by infau-nal forms (morphogroups A4 and A5 – 48%) and forms representing morphogroupA3 – 33%. The suspension feeding forms (morphogroup A1) comprise 10% of theassemblage (Fig. 7).

Thus, these are mainly small dimension fine-grained foraminifera preferring aninfaunal life strategy. Their dominance, together with red colour of sediment, sug-gest aerobic bottom water conditions associated with low organic matter availabil-ity. Such conditions are related to slow sedimentation in a low energy, well-oxygenated and oligotrophic environment. Under low organic matter flux rate theredox boundary layer is in the lower limit of benthic activity in sediment and it pro-vides optimal conditions for epifaunal and shallow to deep infaunal forms (Kuhnt et

al., 1996). In contrast, under high organic matter flux rate the redox boundary layeris close to the sediment-water interface and prevents deep infaunal form expansion.This scenario seems to refer to the sedimentary environment of the shales of the Go-dula beds, which contain foraminifera representing mainly tubular suspensionfeeding forms – 45% (morphogroup A1; Fig. 7). The remaining part of epifaunalforms amount to 32% of the whole benthos. Infaunal forms (morphogroup A5)comprise only 16% of foraminiferal assemblage from the Godula beds. Such an as-semblage, composed predominantly of coarse-grained large-sized foraminifera,suggests a higher flux of organic matter. The occurrence of relatively frequent epi-faunal forms that collected food from the bottom sediment may suggest that sedi-mentation took place under high energy conditions. Low amounts (16%) of infau-nal forms in the greenish coloured shales of the Godula beds indicate low oxygen

268 A. LEMAÑSKA

concentration at the pore waters, depleted presumably due to bacterial decay of or-ganic matter supplied by diluted turbiditic currents.

Discussion

The colour of the sediment depend on several factors: the chemical and mineralcomposition of the sediment, oxygenation of the seafloor, frequency of turbiditesedimentation, thickness and shape of beds, degree and pattern bioturbations. Theyall are strictly connected to one other (Leszczyñski & Uchman, 1991). The red col-our is result from high ratios Fe3+/Fe2+ and the green colour with low ratios (Do-minik, 1977; Potter et al., 1980). The Fe3+/Fe2+ ratio is strongly dependant upon theoxidation state of the sediment. The flux of organic matter is to a large extent re-sponsible for the green coloured shales.

According to the results of this investigation, the morphogroups of the aggluti-nated foraminifera confirm that the green colour is connected with a higher content

CRETACEOUS DEEP-WATER AGGLUTINATED FORAMINIFERA 269

Fig. 7. Distribution of foraminiferal morphogroups (A1–A5) in the variegated shales and Godulabeds

of organic matter, which is expressed by the number of epifaunal forms that collectfood from the bottom sediment. The red colour is expressed by a large proportion ofinfaunal forms indicating better, deeper redox boundary layer, and mesotrophic toeven oligotrophic conditions.

CONCLUSION

(1) Following the standard foraminiferal zonation scheme of Geroch & Nowak(1984), the studied variegated shales can be correlated with the Uvigerinammina

jankoi Zone. The Godula beds can be correlated to the Caudammina gigantea Zone.(2) The age of the variegated shales is Lower Turonian–Lower Santonian, and

the Godula beds are Upper Santonian–Campanian.(3) The foraminifera from the variegated shales are dominated by infaunal,

semi-infaunal forms. This suggests aerobic bottom water conditions associatedwith low organic matter availability. Such conditions are related to slow sedimenta-tion in low energy, well-oxygenated and oligotrophic environment.

(4) The foraminiferal assemblages from the Godula beds are composed of pre-dominantly epifaunal forms, which collected food from the bottom sediment. Itmay suggest that sedimentation took place under high energy conditions, wherefood was supplied by bottom currents, with a relatively higher flux of organicmatter.

Acknowledgments

I would like to thank A. Œl¹czka and A. Gasiñski (Institute of Geological Sciences, JagiellonianUniversity) for discussion on the manuscript. Thanks are due to P. Gedl (Institute of GeologicalSciences, Polish Academy of Sciences) and M. A. Kaminski (UCL) for his comments to themanuscript and improving the English. Thanks are extended to Z. Paul (Polish Geological Institute)for his kind guidance to the field area. Reviews by K. B¹k and J. Tyszka are kindly acknowledged. Thestudy was supported by grant KBN 0444 PO4 2004 26.

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