GeolCarp_Vol52_No6_343

GEOLOGICA CARPATHICA, 52, 6, BRATISLAVA, DECEMBER 2001

343 — 348

TITHONIAN-BERRIASIAN CALPIONELLIDS

FROM THE ŠTRAMBERK-TYPE LIMESTONES, POLISH FLYSCH

CARPATHIANS

TOMASZ CIBOROWSKI

and BOGUSŁAW KOŁODZIEJ

Institute of Oceanography, University of Gdańsk, Al. Marszałka Piłsudskiego 46, 81-378 Gdynia, Poland; tciborow@ocean.univ.gda.pl

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

(Manuscript received January 18, 2001; accepted in revised form June 13, 2001)

Abstract:  Calpionellid  fauna  from  the  coral-bearing  exotics  of  the  Štramberk-type  limestones  from  Polish  Flysch
Carpathians has been studied. Calpionellids of the Remanei Subzone and the Intermedia Subzone as well as the Calpionella
Zone  indicate  the  Late  Tithonian  (most  of  exotics)  and  the  Early  Berriasian  age  of  exotics  studied.  In  contrast  to  the
Štramberk  Limestone  (Moravia),  calpionellids  of  the  Chitinoidella  Zone  have  not  been  recognized  in  the  studied
material.

Key words: Polish Carpathians, Tithonian—Berriasian, Štramberk facies, calpionellids.

Introduction

The best developed Tithonian-Early Berriasian coral reef de-
posits are known from the Štramberk Limestone (Outer Car-
pathians, Moravia – Czech Republic). Great blocks of these
limestones derived from the Baška cordillera occur within
Cretaceous flysch of the Silesian Unit, particularly in the vi-
cinity of Štramberk (Eliáš & Eliášová 1984, 1986).

Within the uppermost Jurassic-Paleogene flysch sequences

of the Polish Flysch (Outer) Carpathians, exotics of the Štram-
berk-type  limestones  occur  as  pebbles,  boulders  and  rarely
klippes.  The  source  areas  of  the  exotic  rocks,  periodically
emerged and eroded, were in continental margins of the Car-
pathian  Basin  and  intrabasinal  ridges  (cordilleras)  separating
particular  sedimentary  basins  (e.g.  Książkiewicz  1965).  The
Štramberk facies both from Moravia and Poland is assumed to
be of Tithonian—Early Berriasian age, however small size and
lack of index fossils in most of exotics make it difficult to es-
tablish the spatial and age relationship between exotics.

Shallow water limestones of Tithonian or Tithonian—Berria-

sian  age  are  also  known  from  other  parts  of  the  Carpathian
range:  Austria  (Ernstbrunn  Limestone),  Hungary,  Romania,
Ukraine (e.g. Patrulius et al. 1976). The term Štramberk-type
limestones is also used for shallow water limestones older than
Tithonian,  for  example,  the  Oxfordian-Tithonian  deposits  of
the Apuseni Mts, Romania (Săsăran et al. 1999).

Analysis of exotics called Štramberk-type limestones from

the Polish Carpathians made by Hoffmann (1992) showed that
they are really developed in various facies reflecting different
environments of sedimentation: from lagoon to basin. Accord-
ing to Hoffmann (1992) coral-microbial reefs were developed
as patch reefs within cortoidal and grapestones facies in an en-
vironment of moderate energy. Apart from corals (Morycowa
1964, 1968, 1974; Kołodziej 1997) microbial structures played
important role in formation of these reefs (Hoffmann 1992;
Hoffmann & Kołodziej 1997).

Material and methods

The studies of calpionellids were based on exotics, which

previously were the subject of coral taxonomy studies
(Kołodziej 1997). Of about 400 pebbles and boulders from 15
localities of the Silesian, Sub-Silesian and Skole units of the
Polish Flysch Carpathians 260 thin sections were made from
96 exotics. The pebbles and boulders studied are usually well
rounded and creamy in colour.

Fig. 1 shows the general position of 7 localities from

which coral-bearing limestones including calpionellids
come. The localities and stratigraphic position of exotics-
containing deposits as well as the museum numbers of exot-
ics discussed in the paper are listed below. Only coral-bear-
ing exotics (see Fig. 2.1) have been taken into consideration.

1 – stream in Leńcze village, 5 km north of Kalwaria Ze-

brzydowska; Lower Istebna Beds (Late Senonian), Silesian
Unit;

2 – Gródek on the Dunajec (Lake Rożnowskie), 15 km

north of Nowy Sącz; Ciężkowice Beds (Eocene), Silesian
Unit;

3 – Krzywa stream in Krzywica village, 7 km west of

Skawina; Verovice Beds (Barremian), Sub-Silesian Unit: exot-
ics UJ 140P/12, UJ 140P/112;

4 – Jastrzębia stream in Jastrzębia village, 1.5 km east of

Lanckorona; Grodziszcze Beds (Early Aptian), Sub-Silesian
Unit: exotic UJ 140P/10;

5 – Rędzina stream in Woźniki village, 6 km north of Wad-

owice; Gaize Beds (Late Aptian—Albian), Sub-Silesian Unit:
exotics UJ 140P/103, UJ 140P/115, UJ 140P/116; UJ 140P/
117 come from black shales within Gaize Beds;

6 – Lipnik Hill (Wapielnica) near Przemyśl, 5 km south-

east of Przemyśl; Ropianka Formation (Inoceramus Beds)
(Maastrichtian—Paleocene), Skole Unit: exotic UJ 140P/14
was collected from the hill in the vicinity of the Kruhel klippe,
now poorly exposed;

344 CIBOROWSKI

and KOŁODZIEJ

7 – Lubeńka stream in Lubenia village, 12 km south of Rz-

eszów; Babica Clays (Late Paleocene), Skole Unit: exotic UJ
140P/1.

Exotics and thin-sections can be found in the collection of

the Institute of Geological Sciences of Jagiellonian University.

Previous study of the stratigraphic position of

Štramberk facies from Moravia and Poland

The age of Štramberk Limestone from Moravia was often

discussed mainly by Czech and Slovak geologists.

Houša (1990), on the basis of calpionellid fauna, stated that

limestones from the Kotouč quarry (Štramberk) can be divided
into two parts. The younger part contains calpionellids belong-
ing  to  Chitinoidella,  Crassicollaria  and  Calpionella  Zones
(without  Calpionella  elliptica  Subzone),  which  indicates  the
age of Late Middle Tithonian—Early Berriasian. The older part
does not contain calpionellids, however, its age has been esti-
mated  as  Early  Tithonian  on  the  basis  of  ammonite  fauna
(Oloriz & Tavera 1982). According to Houša (1990) the basal
part  of  these  limestones  was  formed  during  the  Early  Titho-
nian. The ammonites present in the Štramberk-type limestones
from the uppermost Jurassic-Lower Cretaceous deposits from
the Silesian Unit of Moravia also confirm that sedimentation
of the Štramberk facies continued during the Early Berriasian
(Eliáš & Vašíček 1995).

Recently Houša et al. (1999) have presented the correla-

tion of magnetostratigraphy and calpionellid biostratigraphy
on the Tithonian/Berriasian boundary interval in the Western
Carpathians, including also the Štramberk section (Kotouč
quarry).

Up to now age determinations show that Štramberk-type

limestone  sedimentation  from  the  Polish  Carpathians  is  of
similar age to the Štramberk Limestone. Wójcik (1913, 1914)
on the basis of macrofauna (mainly bivalves, gastropods, am-
monites and brachiopods) determined the age of “coral klippe”
from Kruhel Wielki near Przemyśl as Tithonian and suggested
that  it  can  also  represent  the  Kimmeridgian  and  Berriasian.
Studies  on  calpionellid  fauna  (Geroch  &  Morycowa  1966;
Morycowa  1964,  1988)  indicate  the  Late  Tithonian  age  in
most  of  the  Štramberk-type  limestones  from  Kruhel  (klippe
and pebbles). The study of these authors confirmed Wójcik’s
supposition that some of the limestones were deposited during
the Early Berriasian. According to Morycowa (1988) shallow
water  carbonate  sedimentation  could  persist  locally  till  the
Early  Valanginian.  The  presence  of  calpionellids  pointing  to
Berriasian  age  has  been  determined  by  Morycowa  (1968)  in
exotics  from  vicinity  of  Rożnowskie  Lake.  The  age  of  the
block  from  Woźniki  based  on  calpionellids  and  ammonites
was  determined  as  the  middle  part  of  Late  Tithonian
(Książkiewicz 1974; Morycowa 1974; Kutek 1994), and lime-
stones  from  Inwałd  as  Middle  or  Late  Tithonian  (Nowak
1976).

Discussion on studied calpionellids and

stratigraphical implications

Coral-bearing limestones containing calpionellids represent

biolithites and bioclastic limestones. Calpionellids occur with-
in sediment (biopelmicrite/biopelsparite) between the reefal
fauna or biodetritus. Apart of corals high diversity biota occur,
namely microbial structures, algae, foraminifers, molluscs,

Fig. 1. Geological sketch-map of the Polish Carpathians (simplified after Książkiewicz 1972; Malata et al. 1996) and the localities of the
studied outcrops.

TITHONIAN-BERRIASIAN CALPIONELLIDS FROM ŠTRAMBERK-TYPE LIMESTONES 345

sclerosponges, brachiopods, polychaetes, echinoderms, bryo-
zoans.

Microscopic studies of coral-bearing exotics revealed the

presence of calpionellid fauna in 15 of them. Minute quantities
of calpionellids were found in 6 exotics. Moreover, the ob-
served sections of these specimens were equatorial and ob-
lique, which made their indication impossible. In the case of 9
exotics stratigraphical indication was provided.

Calpionellid fauna occurs in the material studied in a small

amount, but it was able to document the following species:
Crassicollaria intermedia (Durand-Delga 1957); Crassicollar-
ia brevis Remane 1962; Calpionella alpina Lorenz 1902; Tinti-
nopsella carpathica (Murgeanu & Filipescu 1933). As the ma-
terial does not come from the continuous sedimentary section,
the age of the exotics was determined on the calpionellid as-
semblage from the particular exotics. The Rome Standard
Zones (Allemann et al. 1971) were used with their subdivision
in standard subzone according to the Sümeg meeting (Remane
et al. 1986). The most actual biochronological calpionellid zo-

nations (Pop 1997; Reháková & Michalík 1997; Grün & Blau
1997; Remane 1998) were taken into consideration to deter-
mine  the  stratigraphical  position  of  the  particular  exotics.
Moreover,  the  argumentation  of  the  age  determination  was
based  on  important  recent  biostratigraphic  publications  on
calpionellids, namely Houša (1990), Reháková (1995), Lako-
va et al. (1999).

Calpionellid fauna occurring in particular exotics is de-

scribed below along with the interpretation of the stratigraphi-
cal span of the possible stratigraphic position of the exotics
(Fig. 3).

Exotic – UJ 140P/14. The exotic contains the oldest

calpionellid assemblage. Fully hyaline calpionellids belong
to the Remanei Subzone of the Standard Crassicollaria Zone.
Moreover Crassicollaria intermedia has been found. This
form appears in the upper part of the Remanei Subzone (e.g.
Remane 1985; Grün & Blau 1997). The whole calpionellid
assemblage occurring in this exotic pointed to the upper part
of the Remanei Subzone.

Fig. 2. Representative micrographs of the studied material. 1 – general view of coral-bearing limestone with calpionellids; 2 – Crassi-
collaria intermedia, exotic UJ 140P/12; 3 – Calpionella alpina (large form), exotic UJ 140P/1; 4 – Crassicollaria brevis, exotic UJ
140P/1; 5 – Tintinopsella carpathica, exotic UJ 140P/103; 6 – Calpionella alpina (small, sphericular form), exotic UJ 140P/10; 7—9 –
Calpionella alpina (small, spherical form), exotic UJ 140P/112.

346 CIBOROWSKI

and KOŁODZIEJ

Exotic – UJ 140P/12. A similar calpionellid assemblage,

which means specimens of Crassicollaria intermedia (Fig.
2.2) and other Calpionellidae (with fully hyaline wall) was
observed in this exotic. There are also specimens with char-
acteristic crassicollarian collar (described as Crassicollaria
sp.). This suggests the Late Tithonian age, namely the upper
part of the Remanei Subzone, for the examined exotic.

Exotics – UJ 140P/103, UJ 140P/116, UJ 140P/1. In all

these three exotics the age has been determined as Late Ti-
thonian – Intermedia Subzone. Its base is defined by the ap-
pearance of the large form of Calpionella alpina (Remane et
al. 1986). In these three exotics the large form of Calpionella
alpina has been found (Fig. 2.3). Apart from Calpionella al-
pina (large form) specimens, some Crassicollaria sp. (in UJ
140P/103, UJ 140P/116), Crassicollaria brevis (Fig. 2.4; in
UJ 140P/1), Tintinopsella carpathica (Fig. 2.5; in UJ 140P/
103) have been observed. Crassicollaria brevis is typical in
the upper part of the Intermedia Subzone which allows us to
state a more precise age for the exotic UJ 140P/1. Some au-
thors prefer to use the name Calpionella grandalpina Nagy
1986 for the large form of Calpionella alpina, but the taxon-
omy of the genus Calpionella presented by Nagy (1986) is
controversial.

Exotics – UJ 140P/112, UJ 140P/10. Only Calpionella

alpina (small, spherical form) occurs in both of these exotics
(Figs. 2.6—2.9). Their loricas are much smaller and more
globular if compared to Late Tithonian forms. Moreover

these  specimens  are  more  abundant  than  in  Late  Tithonian
exotics. The lower boundary of the Calpionella Zone is de-
termined  on  the  basis  of  the  event,  described  as  an  “explo-
sion” of Calpionella alpina and transition to smaller, globu-
lar forms (Allemann et al. 1971). Considering the size, shape
and  abundance  of  the  occurring  specimens  it  is  possible  to
suggest that the Calpionella alpina specimens belong to the
lower  part  of  the  Calpionella  Zone  –  Calpionella  alpina
Subzone sensu Reháková & Michalík (1997).

Exotics – UJ 140P/115, UJ 140P/117. In the case of

these  exotics  a  minute  quantity  of  Calpionella  alpina  has
been found. The size and shape of the specimens are not con-
clusive  enough  to  determine  the  precise  calpionellid  zone.
The age might be provisionally determined as not older than
the  Intermedia  Subzone.  Specimens  of  Crassicollaria  sp.
found in exotic UJ 140P/115 enable determination of the up-
per boundary for the age of the exotic. It is known that the
occurrence of Crassicollaria sp. is limited to the Crassicol-
laria and Calpionella Zones, however in the upper part of the
Calpionella  Zone  (Vocontian  C  Zone)  Crassicollaria  sp.  is
observed  sporadically  (Remane  1964).  In  the  exotic  UJ
140P/117  Calpionella  alpina  and  Tintinopsella  carpathica
have  been  found.  This  makes  determination  of  the  precise
age impossible. The most approximate determination is the
Calpionella Zone.

In the examined material the calpionellid fauna represent the

Crassicollaria Zone in five cases. In two cases the Remanei

Fig. 3. Calpionellid assemblages occurring in the particular exotics with stratigraphical span of possible stratigraphic position of the ex-
otics (Calpionellid zonation after Remane et al. 1986 – Rome Standard Zones and their subdivision into standard subzones according to
the Sümeg meeting).

TITHONIAN-BERRIASIAN CALPIONELLIDS FROM ŠTRAMBERK-TYPE LIMESTONES 347

Subzone was identified, and in three others the Intermedia
Subzone. In the case of two exotics, calpionellid fauna charac-
teristic for the Calpionella Zone has been observed, suggesting
Early Berriasian age. The age of two other exotics can be esti-
mated as either Late Tithonian (Intermedia Subzone) or Early
Berriasian (Calpionella Zone). In the case of the 6 undescribed
exotics more precise estimation of their stratigraphical posi-
tion was impossible.

According to the literature dealing with the exotics of

Štramberk-type  specimens  of  Crassicollaria  parvula  and
Calpionella  cf.  elliptica  have  been  illustrated  (Morycowa
1968) as well as Calpionella elliptica has been described (e.g.
Morycowa 1964). Both species are characteristic for the upper
part of the Calpionella Zone, which confirms the Middle Ber-
riasian  age  of  some  exotics.  Some  specimens  presented  by
Morycowa (1968, Table IX, Figs. 7, 8, 9, 10, 12) determined
as Calpionellites darderi do not seem to represent this species.
The specimen on the Table IX, Fig. 12 (Morycowa 1968) is al-
most certain to be a specimen from the genus Remaniella. The
present study has not observed Crassicollaria parvula, Calpi-
onella  elliptica  or  Remaniella  in  the  investigated  material,
however,  the  appearance  of  such  calpionellids  has  been  de-
scribed by Morycowa (1964, 1968, 1974).

Generally, the studies on the calpionellid fauna of the exot-

ics  of  Štramberk-type  have  shown  some  similarities  to  the
calpionellid  fauna  occurring  in  allodapic  limestones  of  the
Lower Cieszyn Limestones (basinal equivalent of the Štram-
berk  facies)  from  the  western  part  of  the  Polish  Flysch  Car-
pathians,  where  Crassicollaria  and  Calpionella  Zones  have
been determined (Ciborowski 2000).

Conclusions

Generally, the whole calpionellid fauna occurring in the ma-

terial studied suggests a Late Tithonian—Early Berriasian age
for the Štramberk-type limestones. On the basis of the detailed
studies of exotics, Crassicollaria and Calpionella Zones have
been recognized. Within the Crassicollaria Zone, known from
the  Štramberk  Limestone  (Houša  1990),  Remanei  and  Inter-
media Subzones have been determined by the present authors.
Compared  to  the  calpionellid  zonation  of  Štramberk  Lime-
stone from Moravia (Houša 1990) the present authors have not
observed the Chitinoidella Zone. The youngest examined ex-
otics  show  a  similar  age  to  the  youngest  part  of  Štramberk
Limestone according to the Houša (1990) scheme. However, it
must  be  admitted  that  Calpionella  elliptica  occurring  in  the
Štramberk-type limestones (Morycowa 1964, 1968) suggests
the  possibility  of  extension  of  the  Štramberk  facies  to  the
Calpionella elliptica Subzone.

According to Houša (1990) the thickness of the Štramberk

Limestone in Kotouč quarry close to Štramberk attains 140 m
in the case of the Crassicollaria Zone and 200 m in the case of
the  Calpionella  Zone.  However,  there  is  a  dispute  whether
Štramberk  Limestone  from  the  Kotouč  quarry  exist  as
olistholiths  containing  boulders  and  blocks  belonging  to  dif-
ferent  zones  of  reef  and  different  ages  (Eliáš  1983;  Eliáš  &
Eliášová 1984) or, as presumed by Houša (1983), huge tecton-
ic blocks show internal unity showing the standard succession
of calpionellids.

Both previous works and the study of Štramberk-type lime-

stones stratigraphy from the Polish Carpathians presented here
show mainly Late Tithonian (Crassicollaria Zone) calpionellid
assemblage.

It cannot be excluded that some of exotics called Štramberk-

type limestones from the Polish Flysh Carpathians are older
than Tithonian. According to Malik (1979), analysis of exotics
from the Grodziszcze Beds shows that some exotics contain-
ing corals represent Oxfordian—?Early Tithonian and can be
correlated to the Oxfordian and Kimmeridgian of the Foreland
of the Polish Carpathians, where corals are known (Morycowa
& Moryc 1976).

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