Correlation of the early Albian-late Turonian radiolarian biozonation with planktonic and agglutinated foraminifera zonations in the Pieniny Klippen Belt (Polish Carpathians)

11 Pages·1999·3.4 MB·English

by  Krzysztof Bak

Corrélation of the early Albian-late Turonian
radiolarian biozonation with planktonic and
agglutinated foraminifera zonations in the
Pieniny Klippen Belt (Polish Carpathians)
Marta B/^K
Institute of Geological Sciences, Jagiellonian University,
Oleandry 2a, 30-063 Krakôw (Roland)
[email protected]
Krzysztof BP^K
Institute of Geography, Cracow Pedagogical University,
Podchor^zych 2, 30-084 Krakôw (Roland)
[email protected]
B^k M. & B^k K. 1999. — Corrélation of the early Albian-late Turonian radiolarian biozona¬
tion with planktonic and agglutinated foraminifera zonations in the Pieniny Klippen Belt
(Polish Carpathians), in De Wever P. & Caulel J.-P. (eds), InterRad VIII, Paris/Bierville 8-
13 septembre 1997. Geodiversitas 2^ (4) : 527-537.
ABSTRACT
Marine pelagic deposits of the lower AJbian to upper Turonian inter\'al in
the Polish part of the Pieniny Klippen Belt are relativcly rich in radiolarian
fauna as well as in planktonic and agglutinated foraminifera. The proposcd
KEYWORDS
radiolarian zones (Holoayptocanium barbui^ Hemiayptocapsa prepolyhedra
Cretaceous,
Radiolaria, and Hemicryptocapsa polyhedra) hâve been correlated with planktonic forami¬
Foraminifera, nifera biozonarion (from TidnelUt primula to Dicarinella prhnitiva zone.s),
integrated biostraiigraphy,
and with agglutinated foraminifera biozonation (from Haplophragmoides
Pieniny Klippen Belt,
Carpathians. nonioninoides to Vvigerinarnmma ex ^r.jankoi zones).
RÉSUMÉ
Corrélation des biozones à radiolaires de l'Albien inférieur- furonien supérieur
avec celles à foraminifères planctonicjues et agglutinés dans la région des klippes
piénines (Carpathes polonaises).
Les dépôts marins pélagiques de PAlbien inférieur-Turonien supérieur de la
zone dc.s klippc.s piénines sont relativement riches en faune de radiolaires,
ainsi que de foraminifères planctoniques et agglutinés. Les zones de radio¬
MOTS CLÉS
laires proposées (Holocryptocanium barbais Ifvniicryptoctipsa prepolyhedra cr
Crétacé,
Radiolaria, Hemiciypwcapsa polyhedra) sont en corrélation directe avec les biozones de
Foraminifera, foraminifere.s planctoniques (de la zone Ticinelln primula à la zone
biostratieraphie intégrée,
zone des klippes piénines, Dicarineüa primitiva) et celles des foraminif^res agglutinés (de la zone
Carpathes. Haplophragmoides nonioninoides à la zone Uvigerinammina ex jankoï).
GEODIVERSITAS • 1999 • 21 (4) 527
B^kM. &B^k K.
INTRODUCTION lyses. A detailed description of profiles, sample
location, and lithology is given in papers by
Detailed micropalaeontological studies of marine HL (1992, 1993» 1998) and M. B^k (1995,
pelagic Cretaceous deposirs hâve been carried out 1996a, b, 1997). In 18 of these sections, radiola-
in rhe Picniay Klippen Belt during the last 15 rian skelctons hâve been foimd together with
years. A part of thcse concerncd bioscracigraphy, forarninifera. and thc best sections (15) were
based on differejic groups oFmîcrofauna; forami- used lierc for corrélation purposes (Figs 1,2).
nifera (Birkenmajcr & Jednorowska ]987i In thc sections examined, the microfauna has
Gasihski 1988i Kostka 1993; K. Bi^k 1998), nan- been recovered from rhe deposirs of the
noplankton (Dudziak 1985)» dinoq'srs (Jamihski Kapusnica and Jaworki formations. Liihological
1990) and radiolaria (M. B^k 1995, 1996a, b). features, thickness and âge of these lithostratigra-
However, only very few studies comprise an intc- phical unies, distinguished by Birkenmajer
grated biostraiigraphy of rhese deposirs (1977, 1987), and Birkenmajer 6c Jednorowska
(Birkenmajer Z*/1979; K. BtjkfY^ïZ. 1995). (1984) and presented below, concern only the
The Crccaccous dcposits ol thc Picniny Klippen studied sections.
Bclt providc ihc bcst marctial lor iTc intcgratcd
biostraiigraphical studies in the whole KaPIISNTCA l-OrU'tATKlN
Carparhians, because rhey represenr pelagic and This formation is subdivided in two members,
hemipelagic calcareous-marly faciès, and contain the Brodno Member and the Rudina Member,
abundant micmfauna. These depos’us hâve been both represented in the sections investigated.
formed în the Pieniny Klippen Basin The Brodno Member. Ir has been identified
(Birkcnmajer 1977), a pari of the Penninic only in the one section as a 40 cm thick layer of
Ocean-northcrn part of Western Tethys black maris, ? upper Aprian in âge. The radiola-
(Fourcade étal. 1993) (Fig. lA). The sédimenta¬ rian launa is présent burver)’^ rare in these depo-
tion during Albian thtough Campanian rook sits.
place iindcr deep-water conditions, ar outer shelf The Rudina Member. (1-20 m thick; lower-
through Jower bathyal/abyssal depths, above or upper Albian) It is represented by green-grey and
near CCD (Birkenmajcr & Gasihski 1992; black maris and inarly shales with niarly liniesto-
K. B^k 1995a, b). l'hcy crop oui in a highiy tcc- ne imercalaiions, with red maris appearing in the
tonically deformed zone, known as the Pienîny upper part. Abundant and well-prcserved radio-
Klippen Belt, rhat séparâtes the Innct ftom rhe larian skeletons are présent in green and black
Outer Carparhians (Fig. IB, C)'. maris and niarly shales.
The présent aurhors propose here an integrated
local biostrarigraphy based on planktonic Fora- JAWOKKI POKMAI'ION
minifera, agglutinaicd l'uraminifera and Radio- Deposits of the Jaworki Formation hâve been
laria for early Albian rhrough laie Turonian lime examined in sections belonging to ail Klippen
span. rhe corrélation is based on studies of successions (Fig. 2).
microfauna from the sanie samples wirhin the The Brynczkowa Mari Member. (2-22 m thick;
same sections. Foraminifera and Radiolaria are Vraconian-middle Cenomanian) it consists of
relativcly abundant in the studied deposirs. green or grey-green maris with thin scarce red
mari inrercalation. Moderarely to poorly preser-
ved radiolaria are rare.
GEOLOGIC^\LSETTING AND The Skalski Mari Member. (4-15 m thick;
RADIOLARIAN HORIZONS middie-upper C^cuonvanian) It consisis of varie-
gaced maris, iniercalated with green, red and grey
Twenty five sections locaced at Niedzica, maris. Hxcept of thc Altana Shale Bed, thc radio-
Kroscienko, Szczawnica, Jaworki, Sromowce, larians are présent in this member but are rare
Dursztyn, Szaflary and State Byscre hâve been and mosily poorly preserved.
chosen for integrated micropalaeontological ana¬ The Altana Shale Bed. (0.4-3 ni thick;
528 GEODIVERSITAS • 1999 • 21 (4)
Radiolarian and foraminiferal biozonation in the Pieniny Klippen Belt
Fig. 1. — Location of the study ârea: A, In the Western Tethys {rectangle B) (map of late Cenomanlan palaeoenvironments after
Fourcade et ai 19&3; simplîfied); B. C. in the Carpathians (Pieniny Klippen Bell in black). D. in lhe Pieniny Klippen Belt. Legend. 1.
investigated outcrops; 2. symbols ot outcrops; 3. more important dislocations. List ot outcrops (from west to east): Sb, Stare Bystre;
Ki. Kietowy stream: Sz, Szaflary quarry, Lor Lorencowe Klippes: Csk, Czerwona Skaia, Zt, Ztobowy Creek; Nd. Niedziczanka
slream; Kos, Kosarz.yska Valley; McO Macelowa-Osice; Pg. Podskalnia Gôra ML Mag. Magierowa Klippe; Or. Orlica Hlll: Bw.
Bukowiny Valley: Bd. Bukowiny Hill.
Cenomanian/Turoniaiî boundary) h consists of danc: wcll-preserved siliceous specimens are pré¬
black-blue, grecnish and black shales and marly sent in green and grcy shales and marly shales.
shales. Radiolarians are abundant bur low-diver- The radiolarians arc also abundant in black
sified and poorly preservcd. Their pyritized ske- shales but are often diftlcult to déterminé, becau-
Ictons are mostly found within the Czorsztyn sc of Fe-oxide coating and pyritization.
Succession deposits. The Trawnc Menibcr. (5 m, lowcr-middle
The Magierowa Mari Member. (9 m; Cenomanian) It consists of gre>'-grccn maris and
Cenomanian/Turonian boundar)^ Il is reprcscn- shaly maris with sandstonc intercalations.
icd by shales, marly shales, maris, and thin-bcd- Radiolarian fauna is scarce: only a few poorly
ded marly ümestonc of grey to green colour with preserved specimens bave been found.
black alternations. Radiolarian fauna is abun- The Sneznîca Siltstone Member. (3-? 40 m;
GEODIVERSITAS • 1999 - 21 (4) 529 I
B^k M. & B^k K.
Fig, 2. — Lithological columns of the studied sections in relalion lo the âge of deposits (dashed Itne cortesponds \o the
Cenomanian/Turonian boundary) and tbeir atlnbutton to Klippen successions and sedimenlary zones (Pieniny Klippen Basin recons¬
truction after Birkenmajer (1977)]. Lithological units invesligated |llthoslratlgraphy aller Birkenmajer (1977, 1987), Birkenmajer &
Jednorowska (1984)]: 1, Lorencowe Chert Bed; 2. Osice Siltslone Member; 3, Macelowa and Pusteinia Mari rnenibers 4, Trawne
Member; 5, Sneznica Siltslone Member, 6, Altana Shale Bed; 7, Magierowa Member; 8, Skalski Mari Member; 9, Brynczkowa Mari
Member; 10. Rudina Member: 11, Brodno Member; 12, Pieniny Limestone Formation. Scale bars: 5 m. except of Branisko
Succession sections, 1 m.
GEODIVERSITAS • 1999 - 21 (4)
530
Radiolarian and foraminiferal biozonation in the Pieniny Klippen Belt
middlc Cenomanian-middle Turoiiian) It is rcpre- the familles Actinommidac, Pracconocar)'om-
scntcd by altcrnating bright blue-grey and green midac, Xiphostylidac (gênera Staurosphaeretta
shaly maris widi thin-bcddcd slltstone and sand- and Tviaciomii) y and Dactyliosphaeridae
stone, and bright-grccn pclitic Ümcstonc intercala¬ {Diictyiîodisciis^ Godia and Dactyliosphaera).
tions. Radiohiriims arc raie in this nicmbcr, but Other Spumellaria bclong to the généra
the upper Cenomanian deposirs arc cnriched in Ilexapyrûniis^ Cavdspongla., Pseudoaulophacus,
wcll-preser\’cd, pyi iri/.ed radiolruian skclcron. Patellulû^ Paroniiella and CrucelLi.
The Macelowa Mari Member. (15-70 m; lower Within the Klippen successions investigated, the
Cenomanian-iSantonian) Ir corisists nnjstly of red radiolarians are most abundant and diversificd in
maris and marly Jimesronc vvith thin intercala¬ the Czorsztyn Succession deposits (ourer shelf-
tions of greenish or bltiish siltstones and sand- upper barhyal environment), becoming generally
stones which appcar in its lower and upper parts. scarce in the deposits of the Pieniny Succession
Poorly preserved and mainly calcified radiola- (lower bathyal environments, close to Calcium
rians are présent in this member. They are diver- Compensation Depth).
sified, especially those lound in a horizon The radiolarian specimens are most abundant
corresponding to the lower-middle Turonian. and diverse in green and black marly shalcs,
The Pustelnia Mari Member. (6-45 m; middle maris and limestones ol the Kapusnica and
Cenomanian-Santonian) Ir consists of pure Pomied/nik formations, rhe Magierowa Member
brick-red, strongly lectonized maris wïthout clas- and ihe Aliana Shale Bed of rhe Jaworki
ric intercalations. Radiolarian skcletons are vciy Eorination. Thcy arc scarce in red and variegated
scarcct poorly preservedt and maixily calcified. maris and shales of the Macdowa Mari,
The Lorencowe Chéri Bed. (3 m; upper Brync/kowa Mari and the Skalski Mari members
Santonian-lower Campanian) h is represented by ol the Jaworki Formation. This itilght he dépen¬
a two-meter-thick complex consistiiig of altema- dent on lirhology and iliagenesis factors respon-
ting variegated maris (mostly red) wirh rhin sible for préservation of siliceous microfossils;
intercalations of lighr-green limestone. however, radiolarian fauiias radiarion and turn¬
Radiolarian skeletons are also scarce, poorly pre- overs could be also taken inro account. Both
ser\’'ed, mostly calcified. causes might reflecr an ecological response of
marine biota to global cUmace and sea level
changes during mid-Crctaceous rimes.
RADIOLARIAN ASSEMBLAGES
Two great changes in the radiolarian assemblages
Seventy seven radiolarian species hâve been hâve been retorxied within the srudied deposirs:
determined from the Cretaceous deposics ran- 1. Beginning of an important first radiation of
ging from lower Albian to Santonian of the Radiolaria occurred during the middle Albian
Pieniny Klippen Bclt. 20 gênera and 53 spedes {Ticmella priwula foraminiferal zone» K. Bijk
of Nassellaria, and 11 généra and 24 species of 1992)' as maiiy new species had rheir first appea-
Spumellaria were recognised (M. Bqk 1997). rance in the middlc and rhe lare Albian, The
The assemblages, in ail Klippen successions maximum of différentiation in the radiolarian
mvestigated, are dominated by cryptoccphalic assemblage is obsers^ed in the Vraconian deposits
and cryptothoracic Nassellaria belonging ro the (Rotalipara tidnensis through the Rotalipora
gênera Holocryptoaviiuni^ Hepiicryptocapsa^ appennhiica-Plevwm<tlina huxtorfi foraminiferal
Cryptainphorella. Dorypyle. Hiscocapsa^ zones, K. Bijk 1998). Starting from the upper
Trisyringium and Squirtabollum, Multiscgmcntcd part of the It appennimat-P. hiixtorfi foraminitc-
Nassellaria arc also common being represented ral zone towards the Cenomanian/Turonian
by the gênera Dictyomitra, Thanarla, boundary, a relative decrease in the number of
Pseudodictyomitm^ Stichomitm, Xrtus, Obeliscoites species occurred. As a rcsult, the radiolarian làu-
and Torculum. Spumellaria are less common; the nas in the Czorsztyn, Branisko and Niedzica suc¬
most abundant are the specimens belonging to cessions show great similarities. The same
GEODIVERSITAS • 1999 • 21 (4) 531
B^k M. & B^k K.
characteristic taxa from rhe Riborder Nassellaria the Cenomanian deposits; planktonic Foramini-
(both cryptorhoracic and cryptocep halle forms) fera prcvail there. with dominating rotaliporids,
represented by the généra Holocryplocanium, associated with représentatives of the généra
Hemicryptocapsa, Squinclbollum and Cryptam- Pmeglo ho tru Haï fua Hedbergelht^ Wbile in ella,
phorella arc the most abundant, svhilc the gênera Glvbiga inellûidtSy HcteroheUx and Shuckoina.
Dictyornitray Pseudodictyomiiray Thanarla, Ratio of calcareous to agglutinated bcnihic forms
Stichomitrity Toradumy atul Xitm arc also com- is different in pelagic and hemipelagic deposits of
mon. this stage. Agglutinated taxa prcvail (more than
2. The nexr change in radiolarlan assemblages 80% of benthos) in the scaglia rossa-type
took place around ihe Cenomanian/Turonlan (Macelowa Mari Member) and fivschoid deposits
boundary, Ir surted during the latc Cenomanian (Trawne Member, Sneznica Siltstonc Mentber).
(Rotalipora aishniani loraminiferal 7one, K. B;^k being dominated by Plectorecurvoides tiheruanSy
1998). At that time, dic radiolarlan assemblages Recurvoides sp., Bidbohitcidites sp.. Trochamniina
from tire Picniny Succession becamc similar to sp., Haplophragtnoides sp.. Spiroplecuimminn
those from rhe Czorsztyn, Niedzica and Branisko naparroanriy Arcmlndimina predii, Dorodva sp.,
successions. Moreover, ir was enriched in formvS Triittda sp., Glomospira sp., and by tubular fi^rms.
described so iar only from the Silesian and the Calcareous forms are more frequent in variegated
Skole units of the Outer Flysch Carpathians and red pelagic maris (Brynczkowa Mark Skalski
{Praeconnearyomma lipmanae^ Godia sp., Mari and Fustelnia Mari membets). However,
Diacanthocapsa sp. — sec M. B^k 1994; Corka they are represented by single specimens only.
1996). Agglutinated foraminifers indude the généra
Dentalindy Nodosariay Triitix, Lenticulina,
MarginulinopnSy Mnrginulinay SaYUcenariUy
FORAMINIFERAL ASSEMBLAGES AsîiUùlus. Planulariity Globulinay OolinUy
Pyridimu Rantfdimy huebulimmay P/eurostorneP
The early and middle VVlbian Foraminifera in the la y ValvH U n e ria, Pu lU n ta » (ha ng u la riuy
Pieniny KJippcn Bcit represent a well-diversified GyroidinoideSy Gavelinellay Lingulognvelindla and
assemblage. Planktonk forms prcvail, being Fpnnides.
represented by hedbergellids (//. dtdrioensisy A quilc different foraminiteral assemblage
H. planispira and H. mnplcx)^ Glohgerinelloides appears in black shale faciès close to the
bentoneusis^ and ticincllids (Tidnella primnliiy Cenomatiian/Turonian boundary. Planktonic
T robeni) (k. Bak 1992). Benthos fs dominated Foraminifera are still frequent in the lower part
by cakâreous forms with the most frequent of the shales, being represented predominantly
Gyroidimida inJhureMceay Gavcl/nella cenomam- by Rotalipora cushmanh they are accompanied by
ca and G, interniedia^ and accompanied by whiteinellids, praegiobotruncanids, hedbergeilids
Denîalina sp., Nodosuria sp. and Latticidhja sp. and single form.s from the généra Globigerinel-
Agglutinated foraminifoa {predominantly infau- loules and Heterohflix. In a higher pari ol the
nal forms) are infrequent in rhese deposirs, with shales, only single forms’ of Praeglohotruncana
Dorothia gradata, Xpiroplecfinaîa annectemy delrioensis and Hedbergella detrioensis bave heen
Tritaxüt gatdtma and Textularia foeda prevaillng. found. Benthonic forms are dominated by very
The upper Albian planktonlc Foraminifera are frequent Lenticulina gaultiria. Tliis form is
very numerous and more div'crsified. Besicles the accompanied by single specimens of agglutinated
most frequent hedbetgellids, Bitidnella hreggien- foraminifera from the généra BulhobaculiteSy
sisy PlanornitUna huxtfjrfiy Glabigerinelloides bento- '['rochamminta HarmosinUy Glomospira, Ammo-
nesisy G, ultramicrciy praegiobotruncanids and disais and Rhizammhia.
rotaliporids occur there. Bctuho.s i.s very rare, The middlc-laïc Turoniaii foraminifcral assem¬
dominated by calca^eou^s(cid:9632) forms, similar to those blage considcrably difters from the Cenomanian
présent in the older assemblage. one. Middle furonian was the acme of Helveto-
A very similar assemblage is also characteristic of glohotruncana helvetica and H. praehelvetica
532 GEODIVERSITAS • 1999 • 21 (4)
Radiolarian and foraminiferal biozonation in the Pieniny Klippen Belt
which characterise this assemblage, while ben-
ihonic forms are almost absent. Durlng che late
Turonian, bcnihonic forms bccorae more fre¬
quent, and they prcvail in the latest Turonian
deposiis. rhc bcnthos is dominatcd by aggluti-
nated taxa (more than 90%) with vcty characte*
ri.stic Uvigertnammina jankoi^ Recurvoides
gnduleytsis. GerochitJnmina Cütivena, Kiirrerul'tna
canijonnis, Huplophragmoides c£ bulloides and
Bulhohamlites problematims. Calcarcous benthos
is represented predominantly by the généra
Eponides^ Stensioema and Gyroidinoides.
RADIOLARIAN BIOSTRATIGRAPHY
Radiolarian spccics wcrc idenufied in more than
200 samples from 18 sections in the deposits of
the Pieniny, Branisko, Nicdzica and Czorsznm
successions of the Pieniny Klippen Belt (M. B^k
1997). Scvcntccn horizons containing abundanr
and well-prcscrvcd Radiolaria hâve been chosen
for doser analysis (M. B^k 1999); the Bio-
Graph 2.02 computer program (Savary & Guex
1991) based on the Unitary A-Ssociations Method
was applied. This program produced a scqucnce
of 1 1 U. A. (Hig. 3), which wcrc used for
construcring a radiolarian zonal standard
(M. Bqlc 1999). Three radiolarian zones and five
subzones were proposed for the early Albian
dtrough late Turonian rime span (Fig. 3). These
arc: (1) the Holoayptocttnium barbui zone wilh
Stichornitra Tosilen.sis^ Squinahollum fossile,
Thauitrlü veneUi^ Torcubon dengoi and Oheliscoises
maximus subzones; (2) the Hemicryptoatpsa pre-
polyhedra zone; (3) die Hemwryptoaipsa palyhedm
zone, The top of each zone and subzone is defi-
ned by the FAD of ihe index taxon and aiso by
the base of the overlying zone. Fig, 3. — Occurrence range chan ot index radiolarian apecies
recorded In the Albian to Coniacian deposits in the Pieniny
Klippen Bell successions, based on their first and the last
appearances. and their co-occurrence based on the Unitary
FORAMINIFERAL BIOSTRATIGRAPHY Associations. Abbreviations ot zones: S. tosaensis. Stichomitra
fosaensrs; S. fos., Squinabollum fossile; T. pulch., Thanajia
pulchra, O. maxim,, Obeliscoites rnaximus. 1, local planktonic
Extensive biostratigraphical studies based on foraminiferal zonation atter Robaszynski & Caron (1985) modi-
fied by K. t3a> (1992,1998),
planktonic foraminifera were carried out in
Cretaceous deposirs of the Polish pan of the
Pieniny Klippen Belt (Alexandrowicz 1966; Jednorowska 1987; Kostka 1993). The local bio¬
Alexandrowicz er 1968a, 1968b; Jednorowska zonations hâve been tied to the zonal standards
1979; Gasihski 1983, 1988; Birkenmajer & of the Western Tethys.
GEODIVERSITAS • 1999 • 21 (4) 533
B^kM. &B^k K.
The local planktonic biozonation hcre présentée! d'he définition ol the Holocryplocanium barhui
(K. B^îk 1992, 1998), is based on studies of zone used in this zonation lollows that of
18 field secrion.s (more than 270 samples) repre- Schaaf’s (1985)., with some modification of its
senting deposits from ail sedirnentary zones ol upper limit. The lower boundary of H. hnrbui
the Pieniny KÜppen Basin in Roland. The zones zone {- lowcr boundary of the Stichornitra
distingnished and their chmnostratigraphic cali¬ tûsaensh subzone) is not wcil defined, because the
bration, correspond very well with the Medi- eailicst iAlbian and larest Aptian ( Ticinella wbeni
terranean zona! standard as pioposcd by planktonic loraminifetal zone and Haplo-
Robaszynski Sc Caron (1995), with only minor pbritgnioldes nonioninoides agglutinated loramini-
révision (for more details, see K. B^k 1998). leral zone) deposits arc not well represented in
The biozonation based on agglutinaced foramini- the sections investigated, their radiolarian fuuna
fera foUows that proposed for Outer Carparhians is rare and poorly preserved. d'he upper bounda-
by Geroch & Nowalc (1984), and applied aiso to t)'- ot the H. barhui zone hdls wirhin a lower part
the Pieniny Klippen Bclt (K, B^k ei al. 1995). of the Rotalipora reicheli planktonic foraminiferal
zone and tbc Bulbohaadite^ problrmaticus agglu-
tinafed foraminiteraJ zone (middle Ceno¬
manian). The Sipdnahollum fossile radiolarian
CORRELATION OF RADIOLARAN subzone coiucîdes with the Biticinella bfrggiensis
ZONATION WITH PLANKTONIC AND foraminiferal zone (Late Albian). The Thanarla
AGGLUTINATED FORAMINIFERA ZONES pulthra subzone coincide.s with the Rotalipora
tkinemis-R. subtidnertsis forajninifcral zone (laie
Varions radiolarian zonations for the latc Cieta- Albian). ITc lower limit of the Toradnw deiigoi
ceoLis deposits were proposed depending on the subzone correlates with the upper boundary of
area concerned. Tw'O proposed standards calibra- the Ratalipora tiànvnsiS'R. suhtiçinemis foramini¬
ted with chronostrâtigraphy in the western part feral zone. Its upper limit correlates with the
of the Tethys deserve spécial aaention. d’he first upper boundary ot the Rotalipora appenaimea
standard was proposed by Llumitricâ (1975) for foraminiferal zone (Albian/Cenoinanian bounda¬
the Romanian C'arpachians. Hc rccognised two ry), and also coïncides with the lower limit of the
radiolarian assemblages, the oldei assemblage Obeliscoües maximus subzone.
and the younger one correlatcd with planktonic The lower boundarv' of ihe Hemicryptocapsa pre~
foraminifcr-a. The Holoçryptocaniam barbui- polyhedra zone corresponds to a lower part of the
H. tuberadiitum assemblage corresponds, accor- Rotalipora reicheli planktonic foraminiteral zone
ding to L'iiimitrica (I975}> to the Rotalipora (middle Cenomanian). Its upper boundary
reicheli-R. ci^diwaai7.ont (latest Cenomanian). (= lower boundary of tlîc Pîtrnscrypîovapsa poly¬
O’Dogherty’s (1994) standard was more dctailcd hedra zone) corresponds to an upper pan of the
and compriscd a calibration with the Northern R, cushmani planktonic foraminiferal zone (latc
Apeninnes and Beric Cordillera. l'hLs calibration Cenomanian). I be upper boundary of the
bas been based on planktonic Foraminifera par- H. polyhedra zone bas not been defined within
tially following the zonal standard as proposed by the deposits itwestigated because the Radiolaria
Caron (1985), with some modifications. from the latest Turonian and the Coniacian are
O’Dogherry (1994) recognised five radiolarian very poorly preserved (mosrly calcified). This
zones correlated with the HedbergeUa zone correlates with the Rotalipora cn^hrnani
(Barremiari) through the Marginommeana sigali through Dicarinellay>r;w/oW planktonic fbrami-
(late Turonian) foraminiferal zones. niferal zones ((cid:9632)= upper part ol Bulhohaculites pro-
In this study, wc propose a corrélation of radiola¬ hlematicus and lowcr parc of Uvigerinarmnsna ex
rian zones with planktonic and agglutinaced fora¬ gf. jankoi agglutinated foraminiferal zones; late
miniferal zones for the early Albian rhrough late Cenomanian through late Turonian).
Turonian time span, for the PoHsh part of the It îs hoped that the proposed radiolarian zonal
Pieniny Klippen Belc (Fig. 4). standard will bccome a calibration tool to whicb
534 GEODIVERSITAS • 1999 • 21 (4)
Radiolarian and foraminiferal biozonation in the Pieniny Klippen Bell
LOCAL PLANKTONIC LOCAL RADIOLARIAN
STAGES FORAMINIFERAL BENTHONIC ZONES AND SÜBZONES
ZONES (1) FORAMINIFERAL M. Bak, 1999
ZONES (2)
!9oH Dicarinella primitiva
Marginotruncana sigali
Turonian Uvigerinammina
Helvetogtobotruncana ex gr. jankoi Hemicryptocapsa
polyhedra
helvetica
zone
Praeglobotrvncana delrioensis
Rotalipora cushmani Bulbobaculites
Hemicryptocapsa
Roi.ilipora giùü!ihr4fr,eii^s problematicus
prepolybedra zone
Rotalipora reichell
Cenomanian
Rotalipora
Obeliscoites maximus
globotruncanoides
R appenninica —
-R.appen.^ P.buxt. Torculum dengoi
iooH R buxtorfi-R. ticinensis_
R.ticinensis-R.subticinensis Thanarla pulchra
Biticinella breggiensis Plectorecun/oides Squinabollum fossile
alternans
Ticinella
primula Stichomitra tosaensis
Albian
Haplophragmoides
nonioninoides
(cid:9632) 110^
Ticinella
H
roberti
4
Fig. 4. — Corrélation of radiolarian biozones and subzones with planktonic and agglutinated Foraminifera zonations in the Pieniny
Klippen Belt. PoHsh Carpalhians (chronologicat scale after Robaszynski & Caron (1995)]. 1, local planktonic foraminiferal zonation
after Robaszynski & Caron (1985) modified by K. B^k (1992. 1998): 2. local benthonic foraminiferal zonation after Geroch & Nowak
(1984) modified by K. Bak étal. (1995). K Bak (1995a).
local zonations from orher Carpathian régions vainable éditorial commcnts. Particular thanks
could bc correlated. are due to Prof M. Caron (Institut de Géologie
de rUniversité, Fribourg) and Dr. P. Dunikrica
(Institut de Géologie et Paléontologie^ Université
Acknowledgements de Lausanne) who tcvised the manuscript. Mrs
The authors are greatly indebted to Prof. K. 1. Chodyri (Institute of Geological Sciences,
Birkenmajer (Institute of Geological Sciences, Jagiellonian University, Krakow) helped us in the
Polish Academy of Sciences, Krakow) for laboratory part of the work. This research is a
GEODIVERSITAS * 1999 • 21 (4) 535
B^kM. &B^k K.
contribution of the IGCP 362 Project, Tethyan Btik M. 1993. — l.ute Albian-carly Cenomanian
and Boréal Cretaceous. Radiolaria from rhe Czonszryn Succession, Pieniny
Klippen Belt, Carpathians. Studia Geologica
Polonica 102: 177-20'^.
— 1994- — Radiolaria from Cenomanian deposits of
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