GEOLOGICA CARPATHICA, 52, 4, BRATISLAVA, AUGUST 2001
217—228
JURASSIC SEDIMENTS AND MICROFOSSILS
OF THE ANDRYCHÓW KLIPPES (OUTER WESTERN CARPATHIANS)
BARBARA OLSZEWSKA
1
and JÓZEF WIECZOREK
2
1
Polish Geological Institute Carpathian Branch, ul. Skrzatów 1, 31-560 Krakow, Poland; pigok@pigok.com.pl
2
ul. Smoluchowskiego 4/1, Krakow, Poland
(Manuscript received August 21, 2000; accepted in revised form June 13, 2001)
Abstract: Shallow-water carbonate Jurassic sediments of the Andrychów Klippes (Inwałd, Pańska Góra, Targanice and
Roczyny klippes) differ in origin and environment of deposition from the surrounding flysch complexes. In Jurassic
paleogeography they represented a marginal part of the European Plate (Golonka et al. 2000), the morphology of which
was characterized by the presence of elevated blocks, separated by basins. During Alpine north-directed movements,
several blocks were detached from the continent and incorporated into flysch sediments, mainly in the front of the
Silesian Nappe. Oxfordian cherty limestones of Andrychów Klippes show significant similarities to coeval sediments
deposited on Eurasia’s southern margin. The Tithonian shallow-water limestones with abundant nerineacean-diceratid-
coral fauna, numerous algae (dasycladales, codiaceans, solenoporeaceans), foraminifers (lituolids, miliolids, involutinids)
and calcareous dinocysts show similarities to the Štramberk limestones, and remnants of carbonate sediments of the
European Plate which occur as blocks and exotics in flysch deposits of the Outer Carpathians.
Key words: Carpathians, stratigraphy, Jurassic sediments, carbonate facies, nerineaceans, calcareous dinocysts, algae,
foraminifers.
Introduction
The Andrychów (External) Klippes (Roczyny, Targaniczanka
N, Targaniczanka S, Pańska Góra N, Pańska Góra S, Inwałd
W, Inwałd E) occur in the western part of the Polish Flysch
Carpathians between the localities of Roczyny and Inwałd
(Fig. 1) in a 6 km long zone directed NEE—SWW (Książ-
kiewicz 1935a).
The history of geological investigations of the Andrychów
Klippes covers the span of about 170 years. The first informa-
tion was given by Ami Boue (1830) in his “Observations sur
les Alpes et les Carpathes”. Since that time the Andrychów
Klippes were studied by many geologists and paleontologists
(see Gasiński 1998) trying to resolve their origin and relations
to the surrounding flysch and to the two great bio- and sedi-
mentary provinces: oceanic (Tethyan) and epicontinental
(peri-Tethyan shelf) in the area. The most complete study of
the Andrychów Klippes was made by Książkiewicz (1935
a,b,c) and Nowak (1976, 1983, 1986). The Cretaceous sedi-
ments of Klippes were recently studied by Gasiński (1998).
The present study concentrates on the Jurassic sediments of
Klippes and coincides with the 150th anniversary of the
Zeuschner’s study (1849) of the gastropod faunas of the
Inwałd klippe. In the search for the source area, the relation-
ship of the Andrychów Klippes to the adjacent areas of car-
bonate sedimentation of the region is discussed.
Geological characteristic of the Andrychów Klippes
The Roczyny Klippe. The westernmost and the largest of
the klippes (Książkiewicz 1935a) is composed of Upper Creta-
ceous (conglomerates, crinoidal limestones, marls) and Mid-
dle-Late Jurassic (crinoid and cherty limestones) sediments
and the mylonitized vulcanites. The klippe contacts sediments
of the Silesian and Sub-Silesian nappes (Nowak 1986). The
mutual relationships of the klippe elements were the subject of
contradictory interpretations (Książkiewicz 1935a, 1965;
Nowak 1986).
The Targanice Klippes. The two klippes (N and S) occur in
the Targanice stream valley between the villages of Targanice
and Sułkowice, S from Andrychów. The klippes are separated
by sediments of the Sub-Silesian Nappe (Nowak 1986). The
Northern Targanice klippe is composed of the Upper Creta-
ceous marls, cherty limestones and Lower Paleogene detrital
limestones with Lithothamnium and large foraminifers.
The tectonic interpretation of the Northern Targanice klippe
is very difficult, an imbricated structure is assumed (Nowak
1986).
The much smaller Southern Targanice klippe consists of Up-
per Jurassic cherty limestones and subordinately, Upper Creta-
ceous conglomerates, marls and cherty limestones (Książkie-
wicz 1935b, 1968; Nowak 1986). The Southern Targanice
klippe is an isolated block embedded in the sediments of the
Sub-Silesian Nappe.
The Pańska Góra Klippes. The Pańska Góra klippes occur
as separate blocks at the contact of the Silesian and Sub-Sile-
sian nappes on the northern slope of the Pańska Góra hill (SE
of Andrychów) (Książkiewicz 1935b; Nowak 1986). The
Southern klippe (the biggest one) is formed by Upper Creta-
ceous marls, Paleogene dark shales and limestones and subor-
dinately, by crystalline rocks and Upper Jurassic limestones.
The Northern klippe, a block of granite-gneiss, is wedged up
in the Krosno Beds of the Sub-Silesian Nappe. The Western
218 OLSZEWSKA
and WIECZOREK
klippe (the smallest one) is composed of tectonized crystalline
rocks and a small fragment of Paleogene limestones (Nowak
1986).
The Inwałd Klippes. Nowak (1986) described two Inwałd
klippes, one of them being rather a set of blocks grouped
around so called “main klippe” (the E Inwałd klippe), another,
an isolated block (the W Inwałd klippe). The klippes outcrop
in several abandoned quarries at the foot of the Wapienica hill
S of Inwałd (Książkiewicz 1935a). They contact both the Sile-
sian and the Sub-Silesian nappes (Książkiewicz 197l;
Książkiewicz & Liszkowa 1972; Nowak 1986; Gasiński
1998). The Eastern klippe is composed of Upper Jurassic lime-
stones (with the famous Nerinea fauna described by
Zeuschner 1849), Upper Cretaceous marls and mudstones, Pa-
leogene limestones and mylonitized granite gneisses (Nowak
1986; Gasiński 1998). The Western klippe is composed exclu-
sively of mylonitized granitic rock.
Distribution of fossils in sections studied
The Roczyny Klippe. Three types of Jurassic limestones
are known from the Roczyny klippe: crinoidal limestones,
cherty limestones and so called “Inwałd-type limestones”
(Książkiewicz 1935a; Nowak 1986). Crinoidal limestones oc-
curs in isolated blocks. Thin sections reveal their packstone
texture with dense packed crinoid stems, bryozoans, ostracods
and rare foraminifers. The lack of stratigraphically significant
fossils makes proper age designation difficult. Most frequently
they were attributed to the late Middle Jurassic (Książkiewicz
1935a, 1968).
Cherty limestones were found both in the surface outcrop
(Książkiewicz 1935a; the author’s studies) and in the Roczyny
6 borehole (Książkiewicz & Liszkowa 1972). The micritic
limestones contain foraminifers: Epistomina sp., Globuligeri-
na cf. oxfordiana Grigelis, Paalzowella turbinella Gümbel,
Opthalmidium aff. strumosum (Gümbel), abundant sponge sp-
icules, fragments of echinoderms and calcareous dinocysts:
Colomisphaera fibrata (Nagy), Crustocadosina semiradiata
(Wanner). They were attributed to the Lower-Middle Oxford-
ian which supports earlier age designations (Książkiewicz &
Liszkowa 1972).
The “Inwałd limestones” (bioclastic grainstone) contain nu-
merous organic remnants: thin sections investigated contained
foraminifers – Quinqueloculina cf. verbizhiensis Dulub,
Mohlerina basiliensis (Mohler), Protopeneroplis cf. striata
Weynschenk, Spirillina sp., Lenticulina sp., Globuligerina sp.;
zoospores (Globochaete alpina Lombard), microproblematics
(Tubiphytes cf. morronensis Crescenti), isolated sections of
calpionelids (presumably Crassicollaria), gastropods (Ptyg-
matis pseudobruntrutana mentioned by Zeuschner 1849),
echinoderms, and also microoncoids and ooids. The assem-
blage suggests an Upper Tithonian age and a shallow, near reef
environment of the sediments investigated.
The Targanice Klippes. The Jurassic cherty limestones
(cherty grainstones) outcrops in the Southern klippe. Bioclasts
are composed of foraminifers: Globuligerina cf. oxfordiana
Grigelis, Protomarssonella jurassica (Mitjanina), Glomospira
variabilis Kübler et Zwingli, Protopeneroplis striata Weyn-
schenk, Opthalmidium aff. marginata Wiśniowski, Paalzowel-
la sp., Lenticulina sp., Spirillina sp.; calcareous dinocysts: Ca-
dosina parvula Nagy; microproblematics; Koskinobullina
Fig. 1. Location of the Andrychów Klippes in relation to the other profiles of Jurassic sediments.
JURASSIC SEDIMENTS AND MICROFOSSILS OF ANDRYCHÓW KLIPPES 219
socialis Cherchi et Schroeder; calcified radiolarians, sponge
spicules, rare secundibranchia of Saccocoma sp.
The assemblage resembles typical Lower-Middle Oxfordian
microfossil assemblages from the southern part of the Eurasian
Plate underlying the Outer Carpathians (Golonka 1978;
Matyszkiewicz 1997; Olszewska 1998), and probably repre-
sents the same age and open sea environment.
The Pańska Góra Klippes. The Jurassic cherty limestones
(grainstones) occur in the Southern klippe. The microfossil
content is similar to that already reported from this type of
rock. Foraminifers are represented mainly by arenaceous spe-
cies: Textulariopsis jurassica (Gümbel), Reophax helveticus
Haeussler, Glomospira variabilis Kübler et Zwingli. Rare cal-
careous species belong to Istriloculina fabaria Matsieva et
Temirbekova. Książkiewicz (1935b) reports numerous sponge
spicules in investigated samples. This was also verified during
recent studies.
The Inwałd Klippes. The Jurassic limestones occur mainly
in the Eastern klippe. This is a yellowish or whitish massive,
poorly bedded limestone with abundant nerineacean-dicer-
atids-coral fauna. Zeuschner (1849) described from the lime-
stones: Cryptoplocus depressus (Voltz), Ptygmatis pseudo-
bruntrutana (Bronn), Ptygmatis carpathica (Zeuschner),
?Diptyxis
crispa
(Zeuschner),
?Endoplocus
staszycii
(Zeuschner), ?Eunerinea hoheneggeri (revised names!).
The “Inwałd limestones” are also rich in microfossils, espe-
cially foraminifers, calcareous algae and calcareous dinocysts.
Foraminifers form an assemblage associated with a reefal envi-
ronment. The most frequent species include: Pseudocyclammi-
na lituus (Yoko) Yokoyama, Valvulina alpina Dragastan, V. lu-
geoni
Septfontaine,
Protomarssonella
cf.
dumortieri
(Schwager), Paleogaudryina cf. varsoviensis (Bielecka et
Pożaryski), Mohlerina basiliensis (Mohler), Quinqueloculina
mitchurini Dain, Quinqueloculina verbizhiensis Dulub, Quin-
queloculina stellata Matsieva et Temirbekova, Istriloculina fa-
baria Matsieva et Temirbekova, Scythiloculina confusa Neagu,
Trocholina alpina (Leupold), Andersenolina perconigi Neagu,
A. elongata (Leupold), Spiroloculina cf. subpanda Lloyd,
Nautiloculina cf. cretacea Peybernes, Protopeneroplis ultra-
granulata (Gorbatchik), P. striata Weynschenk, Charentia evo-
luta (Gorbatchik) (Fig. 3).
The algal association consists of: Salpingoporella annulata
Carozzi, Salpingoporella ex gr. pygmaea (Gümbel), Actinopo-
rella podolica Alth, Clypeina jurassica Favre, Eoteutloporella
socialis (Praturlon), Thaumatporella parvovesiculifera Rain-
ieri, Baccinella irregularis (Radoicic), Lithocodium aggrega-
tum Elliott, Alpinella distincta Dragastan, Hedstroemia mold-
avica Dragastan (Fig. 5).
The calcareous dinocysts are represented by: Carpistomi-
osphaera tithonica Nowak, Colomisphaera carpathica (Bor-
za), Colomisphaera ornata Nowak, Stomiosphaera molucca-
na Wanner, Cadosina fusca Wanner, Cadosina parvula Nagy
(Fig. 4).
From the thin bedded part of the massive limestones
Książkiewicz (1971) reports numerous secundibranchia of
Saccocoma Agassiz indicating proximity of the open sea.
The age of the “Inwałd limestones” based on foraminifers
and the calcareous dinocysts as well as nerineaceans is Late
Tithonian in the type locality.
In the Inwałd 5 borehole, the “Inwałd limestones” show
traces of dolomitization (Książkiewicz & Liszkowa 1972).
The significance of the microfossil assemblages
for the interpretation of the Jurassic sequence
of the Andrychów Klippes
Three main types of Jurassic limestones can be recognized
in the Andrychów Klippes:
1 – the crinoidal limestones, 2 – the cherty limestones,
3 – the “Inwałd limestones”.
They vary in age, microfossil content and the environment
of deposition.
1. The crinoidal limestones (the Roczyny klippe). The
crinoidal packstone. The lack of stratigraphically significant
fossils precludes proper designation of age. However, Callov-
ian age is very probable. The limestones are generally attribut-
ed to a quiet environment with a water depth of several tens of
metres (Mišík 1974).
2. The cherty limestones (the Roczyny klippe, S Targanice
klippe, S Pańska Góra klippe). The microfossil assemblage
consists of foraminifers, calcareous dinocysts, sponge spi-
cules, calcified radiolarians and rare secundibranchia of Sac-
cocoma Agassiz. Foraminifers are represented by Glomospira
Fig. 2. Situation of the Tithonian Inwałd elevation on the Eurasian margin of Northern Tethys and possible location of the late Alpine
(Middle Miocene) detachment planes.
220 OLSZEWSKA
and WIECZOREK
variabilis Kübler et Zwingli, Textulariopsis jurassica (Güm-
bel), Protomarssonella jurassica (Mityanina), Paalzowella
turbinella Gümbel, Vinelloidea crussolensis Canu, Protopen-
eroplis striata Weynschenk, Globuligerina oxfordiana Grige-
lis, Ophthalmidium sp., Spirillina sp., Epistomina sp., Lenticu-
lina sp. The assemblage resembles Oxfordian foraminiferal
faunas known from the carbonate sediments of peripheral parts
of the Eurasian Plate (Moryc & Morycowa 1976; Hanzliková
& Bosák 1977; Golonka 1978; Eliáš & Eliášová 1984; Olsze-
wska 1998). The calcareous dinocysts are rare but significant;
Colomisphaera fibrata (Nagy), Crustocadosina semiradiata
(Vogler), Cadosina parvula Nagy indicate the Early-early Late
Oxfordian age (C. fibrata Zone) of cherty limestones of the
Andrychów Klippes (Garlicka 1974; Garlicka & Tarkowski
1980; Řehánek & Heliasz 1993). Foraminifers, calcareous di-
nocysts, radiolarians and Saccocoma ossicles indicate the sub-
littoral environment, probably connected with the progressing
Oxfordian transgression (Golonka 1978; Matyszkiewicz
1996).
3. The “Inwałd limestones” (Inwałd klippe, Roczyny
klippe). The characteristic foraminiferal assemblage consists
of: Pseudocyclammina lituus (Yokoyama), Valvulina alpina
Dragastan, V. lugeoni Septfontaine, Protomarssonella cf. du-
mortieri (Schwager), Palaeogaudryina varsoviensis (Bielecka
et Pożaryski), Quinqueloculina mitchurini Dain, Q. stellata
Matsieva et Temirbekova Istriloculina fabaria Matsieva et
Temirbekova, Decussoloculina barbui Neagu, Scythiloculina
confusa Neagu, Trocholina alpina (Leupold), T. burlini Gor-
batchik, Andersenolina perconigi Neagu, A. elongata (Le-
upold). Other common species include: Mohlerina basiliensis
(Mohler), Nautiloculina oolithica Mohler, N. cf. cretacea Pey-
bernes, Protopeneroplis ultragranulata (Gorbatchik), P. stria-
ta Weynschenk, Charentia evoluta Gorbatchik, Pfenderina sp.
They are characteristic for the peri-reefal and the intraplatform
environments with prevalence of the latter. The stratigraphic
distribution of the selected species (N. cretacea, P. ultragranu-
lata) suggests at least a Late Tithonian age for the Inwałd
limestones.
The algal association of the “Inwałd limestones” is com-
posed of dasycladales: Actinoporella podolica (Alth), Clypei-
na jurassica Favre (rare), Salpingoporella annulata Carozzi,
S. pygmaea (Gümbel), Eoteutloporella socialis (Praturlon);
encrusting codiaceans: Baccinella irregularis Radoicic, Li-
thocodium aggregatum Elliot; encrusting solenoporaceans:
Thaumatoporella parvovesiculifera Rainieri and rare cyano-
phyceans Rivularia sp.; microproblematics: Koskinobullina
socialis Cherchi et Schroeder. Outer platform elements gener-
ally prevail with encrusting and high energy forms that proba-
bly fell down from the biostromes of the shelf margin (Flügel
1979; Dragastan 1980; Řehánek 1987; Soták & Mišík 1997).
This supports Książkiewicz’s (1971) view indicating a “slop-
ing bottom” as the site of deposition of the Inwałd limestones.
The calcareous dinocysts: Colomisphaera carpathica Borza,
C. cieszynica Nowak, Carpistomiosphaera tithonica Nowak,
Cadosina parvula Nagy, Stomiosphaera moluccana Wanner.
represent the Middle-Late Tithonian C. carpathica-C. cieszyni-
ca Zone (Nowak 1968). Sections of unidentified calpionellids
are also present.
The Saccocoma rich layer described by Książkiewicz
(1971) from the bottom of the Inwałd limestones in the type
locality can be correlated with the Kimmeridgian/Tithonian
mass occurrences of these crinoids known from the Tethys
(Borza 1969; Keupp & Matyszkiewicz 1997) only on the basis
of their position in the profile.
Correlation with coeval microfossil assemblages of
other carbonate sedimentation areas of the region
1. In the early 50-ties in the Bachowice wood (East of the
Andrychów Klippes) Książkiewicz (1956) explored layers
with exotics embedded in variegated Paleogene shales of the
Sub-Silesian Nappe. Apart from exotic crystalline rocks an
impressive number of sedimentary rocks was collected from
artificial exposures. They covered the time span from Carbon-
iferous (Tournaisian) to Cretaceous (Maastrichtian). Among
these rocks those containing Tithonian fossils were common.
Blocks of pale cryptocrystalline limestones contained frequent
ammonite remains, small pebbles were made of whitish or yel-
lowish Calpionella limestones with Crassicollaria parvula
Remane, Crassicollaria brevis Remane, Calpionella alpina
Lorenz. The Calpionella limestones also contained foramini-
fers, radiolarians, zoospores, and algae (Fig. 6). Recent inves-
tigations (Malata & Olszewska 1998) additionally revealed the
presence of the calcareous dinocysts, among others: Co-
mittosphaera pulla (Borza), Colomisphaera lucida Borza, Co-
lomisphaera lapidosa (Vogler). The prevalence of the pelagic
elements in the Tithonian sediments of the Bachowice succes-
sion indicates an open sea environment. Książkiewicz reports
only one fragment of rock (oolitic-crinoidal limestones) that
may represent neritic, peri-reefal facies similar to the “Inwałd
limestones”. Thus the Bachowice Tithonian sediments accu-
mulated mainly in pelagic, open sea environment different
from that where sediments of the Andrychów Klippes were
deposited.
2. Interesting hints referring to the origin of the Andrychów
Klippes come from the investigations of strata and fossils of
the peri-Tethyan shelf submerged under the Outer Carpathians
(well Zagórzyce 6) or incorporated into flysch deposits as
olistholiths (Kruhel klippe).
Well Zagorzyce 6 situated at the marginal part of the Skole
Nappe (Fig. 1) reached Tithonian-earliest Berriasian deposits
(the Ropczyce Series) at the depth of 2810 m (Olszewska
1999). The Tithonian sediments show regressive character and
are composed of hypersaline lagoon deposits with coprolithes
(Favreina sp.) and Charophyta (Clavatoraceae). Alternating
normal marine layers contain foraminifers (Pseudocyclammi-
na lituus (Yokoyama), Miliolidae), algae, mainly dasyclads
(Salpingoporella pygmaea (Gümbel)), or codiaceans (Hed-
stroemia moldavica Dragastan, Pratumiella fastigiata Dra-
gastan, Clypeina jurassica Favre), calcareous dinocysts (Ca-
dosina fusca Wanner, Comittosphaera pulla (Borza),
Crustocadosina semiradiata (Wanner)) and single capionel-
lids (Calpionella alpina Lorenz) (Fig. 7).
Olistholiths of Jurassic rocks embedded in the Inoceramian
Beds of the Skole Nappe at Kruhel (S from Przemyśl) yielded
similar assemblage of microfossils (Fig. 8). More frequent
calpionellids are represented by: Crassicollaria brevis Re-
mane, Crassicollaria intermedia (Durand Delga), Tintinopsel-
la cf. carpathica (Murgeanu et Filipescu), Tintinopsella suba-
JURASSIC SEDIMENTS AND MICROFOSSILS OF ANDRYCHÓW KLIPPES 221
Fig. 3. Characteristic foraminifers of the Inwałd limestones. 1 – Charentia evoluta (Gorbatchik), axial section; scale bar = 0.09 mm. 2
– Charentia evoluta (Gorbatchik), equatorial section; scale bar = 0.09 mm. 3 – Andersenolina perconigi Neagu, subaxial section; scale
bar = 0.03 mm. 4 – Trocholina alpina (Leupold), subaxial section; scale bar = 0.017 mm. 5 – Pseudocyclammina lituus (Yokoyama),
transverse section; scale bar = 0.09 mm. 6 – Mohlerina basiliensis (Mohler), oblique section; scale bar = 0.09 mm. 7 – Protopeneroplis
striata Weynschenk, subaxial section; scale bar = 0.08 mm. 8 – Scythiloculina confusa Neagu, transverse section; scale bar = 0.07 mm.
9 – Scythiloculina confusa Neagu, longitudinal section; scale bar = 0.07 mm.
222 OLSZEWSKA
and WIECZOREK
Fig. 4. Characteristic calcareous dinocysts of the Inwałd limestones. 1 – Carpistomiosphaera tithonica Nowak; scale bar = 0.01 mm. 2 –
Carpistomiosphaera tithonica Nowak; scale bar = 0.008 mm. 3 – Carpistomiosphaera borzai (Nagy); scale bar = 0.008 mm. 4 – Colo-
misphaera carpathica (Borza); scale bar = 0.008 mm. 5 – Comittosphaera sublapidosa (Vogler); scale bar = 008 mm. 6 – Crustocadosina
semiradiata (Wanner); scale bar = 0.008 mm. 7 – Stomiosphaera moluccana Wanner; scale bar = 0.007 mm. 8 – Cadosina parvula Nagy;
scale bar = 0.007 mm.
JURASSIC SEDIMENTS AND MICROFOSSILS OF ANDRYCHÓW KLIPPES 223
Fig. 5. Characteristic calcareous algae of Inwałd limestones. 1 – Baccinella irregularis Radoicic. 2 – Alpinella distincta Dragastan. 3
– Thaumatoporella parvovesiculifera (Raineri). 4 – Salpingoporella ex gr. pygmaea (Gümbel). 5 – Lithocodium aggregatum Elliott.
6 – Eoteutloporella socialis (Praturlon). 7 – Salpingoporella annulata Carozzi. Scale bar = 0.08 mm in 1—7.
224 OLSZEWSKA
and WIECZOREK
Fig. 6. Characteristic microfossils of the Tithonian sediments of Bachowice Succession. 1 – Calpionella alpina Lorenz and Comittosphaera
sublapidosa (Vogler); scale bar = 0.015 mm. 2 – Crassicollaria parvula Remane; scale bar = 0.015 mm. 3 – Comittosphaera pulla (Bor-
za); scale bar = 0.008 mm. 4 – Colomisphaera lucida Borza; scale bar = 0.004 mm. 5 – Colomisphaera lapidosa (Vogler); scale bar =
0.008 mm. 6 – Globochaete alpina (Lombard); scale bar = 0.03 mm. 7 – Calpionella limestones and Aptychi; scale bar = 0.09 mm. 8 –
Saccocoma sp. Agassiz; scale bar = 0.035 mm.
JURASSIC SEDIMENTS AND MICROFOSSILS OF ANDRYCHÓW KLIPPES 225
Fig. 7. Characteristic microfossils from the Tithonian-earliest Beriassian sediments of the marginal part of the Eurasian Plate in Zagórzyce 6
well. 1 – Charophyta (?Clavator sp.), transverse stem section; scale bar = 0.017 mm. 2 – Coprolites (Favreina sp.), transverse section;
scale bar = 0.035 mm. 3 – Clypeina jurassica Favre; scale bar = 0.035 mm. 4 – Crustocadosina semiradiata (Wanner); scale bar = 0.008
mm. 5 – Pseudocyclammina lituus (Yokoyama), transverse section; scale bar = 0.09 mm. 6 – Calpionella alpina Lorenz; scale bar = 0.017
mm. 7 – Quinqueloculina mitchurini Dain, transverse section; scale bar = 0.075 mm. 8 – Quinqueloculina mitchurini Dain, longitudinal
section; scale bar = 0.075 mm.
226 OLSZEWSKA
and WIECZOREK
Fig. 8. Characteristic microfossils of the Tithonian sediments of the Kruhel klippe. 1 – Crassicollaria brevis Remane; scale bar = 0.017
mm. 2 – Crassicollaria intermedia (Durand Delga); scale bar = 0.017 mm. 3 – Decussoloculina barbui Neagu, transverse section; scale
bar = 0.08 mm. 4 – Trocholina molesta Gorbatchik, subaxial section; scale bar = 0.034 mm. 5 – Actinoporella podolica Alth; scale bar =
0.034 mm. 6 – Tubiphytes sp.; scale bar = 0.09 mm. 7 – Charophyta; scale bar = 0.08 mm. 8 – Colomisphaera carpathica (Borza); scale
bar = 0.009 mm.
JURASSIC SEDIMENTS AND MICROFOSSILS OF ANDRYCHÓW KLIPPES 227
cuta (Colom), Calpionella alpina Lorenz, (Geroch et Mory-
cowa 1966; authors investigations). Among foraminifers the
following are frequent: Protomarssonella hechti (Dieni et
Massari), Trocholina burlini Gorbatchik, Protopeneroplis ul-
traganulata (Gorbatchik), Andersenolina delphinensis (Ar-
naud Vanneau, Boisseau, Darsac), Troglotella incrustans
Wernli et Fookes, Miliolidae. Algae are represented by dasy-
cladales: Actinoporella podolica Alth, Salpingoporella annu-
lata Carozzi, Lithocodium aggregatum Elliott, and Charophy-
ta. Colomisphaera carpathica (Borza) (Fig. 8) is frequent in
the calcareous dinocyst assemblage.
Compared to microfossils of the Andrychów Klippes peri-
Tethyan shelf assemblages are more environmentally diversi-
fied, probably due to different localization of investigated sites
on the margin of European Plate. Local abundance of calpi-
onellids (Kruhel klippe) indicates that some sites were situated
closer to ducts that distributed pelagic elements on the plat-
form (Danian-Polish seaway).
Andrychów Klippes – elevated blocks of the rifted
Jurassic sediments of the Eurasian margin
Both rock types and the fossil content of the Late Jurassic
sequences of Andrychów Klippes show strong silimarities to
coeval sediments and faunas of the southern margin of the
Eurasian Plate. Oxfordian cherty limestones show significant
correlation to coeval sediments known from the Brno area,
Cracow Upland, Carpathian basement, Southern Ukraine. Mi-
crofossil assemblages contain the same species of foramini-
fers, calcareous dinocysts and calcareous algae.
Tithonian shallow water limestones (the “Inwałd lime-
stones”) with abundant nerineacean-diceratid-coral fauna, nu-
merous algae (dasycladales, codiaceans, solenoporaceans) and
foraminifers (lituolids, miliolids, involutinids) are similar to
Štramberk-type reefal limestones frequently found in flysch
sediments of the Outer Carpathians and Waschberg Zone of
Austrian Alps (Blaschke 1911; Bachmayer 1961; Eliáš &
Eliášová 1984; Řehánek 1987; Wieczorek 1988, 1998; Wójcik
1914; Zittel 1873).
The “Inwałd limestones” also resemble Tithonian deposits
of the European Plate found in Zagorzyce 6 well (Olszewska
1998) under the Skole Nappe of the Outer Carpathians. At the
surface similar shallow water Tithonian limestones, with
nerineaceans, algae and peri-reefal foraminifers, is known
from the Niżniow Formation in Ukraine (Alth 1882; Dulub et
al. 1986).
In the present state of our knowledge of Tithonian paleo-
geography, it is justified to interpret the Andrychów Klippes
(Fig. 2) as elevated blocks, which separated the Bachowice ba-
sin in the outer position and the Silesian pull-apart (?) basin in
the inner position (Książkiewicz 1956; Nowak 1976; Matysz-
kiewicz & Slomka 1994). This topography resulted from ini-
tial disintegration of the Southern margin of the Eurasian Plate
related to, probably oblique, rifting processes.
During Alpine north-directed movements block fragments
were detached from the Eurasian Plate and incorporated into
flysch deposits, mainly in front of the Silesian Nappe.
Acknowledgments: The authors are much indebted to: Prof.
O. Dragastan (University of Bucharest, Romania), Prof. I. Bu-
cur (University Babe Bolayi, Romania) for help in identifying
algae; Dr. D. Rehaková (Slovak Academy of Sciences, Brat-
islava) for discussion concerning calpionellids and calcareous
dinocysts of Carpathians; Dr. N. Grambast-Fessard (Univer-
sité des Sciences et Techniques du Languedoc, France) for
consultation concerning Charophytes.
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