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, AUGUST 2015, 66, 4, 285—302 doi: 10.1515/geoca-2015-0026
Introduction
During the Laramian movements, the sedimentary nappes
which constitute the Pieniny Klippen Belt (PKB), a narrow
and elongated tectonic zone situated on the northern flank of
the Central Western Carpathians (a part of the Alpide belt)
(Fig. 1), were stripped off from their basement and stacked at
the front of the propagating thrust (Birkenmajer 1986). These
structures were subsequently redeformed during the Miocene,
when the turbiditic basins of the Outer Carpathians were clos-
ing and the original spatial arrangement of the depositional
succession was distorted (see Jurewicz 2005). The intensity of
the wrench tectonics led to the spatial complexity of the belt’s
structure, expressed in an apparently chaotic distribution of
rigid rock complexes (“Klippen”) within the crumpled, less
rigid shaly sediments. Therefore, the sequences dominated by
shales and marls (such as the one described in this paper) tend
to be strongly disturbed and incomplete. However, the strati-
graphy and paleogeographic position of marly sediments with
turbidites is of high importance in assessing the structural
evolution of the Pieniny Klippen Belt during the Mesozoic
because they can be used to infer the timing of the major sea-
floor differentiation in the PKB. Such is the case of a Middle
Jurassic succession comprising the turbiditic Szlachtowa
Formation, examined and discussed herein within a context
of the Czorsztyn Ridge development.
The stratigraphic and structural position of the deposits of
the Szlachtowa Formation (the so-called “black flysch”),
The Middle Jurassic succession in the central sector of
the Pieniny Klippen Belt (Sprzycne Creek): implications for
the timing of the Czorsztyn Ridge development
TOMASZ SEGIT
1
, BRONISŁAW A. MATYJA
1
and ANDRZEJ WIERZBOWSKI
2
1
Institute of Geology, University of Warsaw, Żwirki i Wigury 93, 02-089 Warszawa, Poland; t.segit@uw.edu.pl; matyja@uw.edu.pl
2
Polish Geological Institute – National Research Institute, Rakowiecka 4, 00-975 Warszawa, Poland; andrzej.wierzbowski@pgi.gov.pl
(Manuscript received November 22, 2014; accepted in revised form June 23, 2015)
Abstract: In this study, we revisit the stratigraphic age and discuss sedimentary characteristics of the lower Middle
Jurassic turbidite deposits (“black flysch”) of the Szlachtowa Formation, as well as the under- and overlying members of
the Sprzycne Creek section situated in the central sector of the Pieniny Klippen Belt (Poland). We show that the succession
captures the lower Middle Jurassic marine sediments of the pre-Late Albian Magura Basin, located to the north of an
ancient submarine swell (Czorsztyn Ridge). The turbidite deposits of the Szlachtowa Formation and marly shales of the
Opaleniec Formation yield dinoflagellate cysts indicative of the latest Aalenian or learliest Bajocian to Early Bathonian.
The character of these deposits, and their location below the overthrusted Subpieniny Nappe show that this succession does
not belong to the successions of the Oravicum domain, located on the southern side of the Czorsztyn Ridge. The Szlachtowa
Formation is underlain by the Skrzypny Formation, which is reported for the first time outside the Oravicum domain. It
suggests that the pre-Late Albian Magura Basin came into existence not earlier than during the latest Aalenian, following
the rising of the Czorsztyn Ridge. The marly shales assigned here to the Opaleniec Formation of Late Bajocian-Bathonian
age and younger marly deposits of Cretaceous age were distinguished in the past as the so-called “Sprzycne beds” of
Cretaceous age. However, the combination of these two rock units into a single lithostratigraphic unit is unsuitable because
they represent two separated stratigraphical intervals and their contact is tectonic.
Key words: Middle Jurassic, Pieniny Klippen Belt, Magura Basin, “black flysch”, stratigraphy, dinoflagellate cysts.
represented by the black micaceous shales with intercala-
tions of sandstones and allodapic crinoidal limestones, have
been subject to controversial interpretations over the years.
These deposits were stratigraphically attributed either to cer-
tain parts of the Early—early Middle Jurassic interval, namely
the Upper Toarcian—lowermost Aalenian (Birkenmajer
1977), Upper Toarcian—Upper Bajocian (Gedl 2008a; in-
cluding a hiatus spanning the uppermost Toarcian/Lower
Aalenian to lower Upper Aalenian), Lower Bajocian (Barski
et al. 2012; base and top of the formation unknown),
?Middle/Upper Toarcian—Middle Bathonian (Gedl & Józsa
2015), or, by contrast, to the middle Cretaceous (Albian—
Cenomanian) (e.g. Sikora 1971c; Oszczypko et al. 2004,
2012). Due to tectonic perturbations, the base of the forma-
tion has remained enigmatic until now. On the other hand,
the sedimentary area of the Szlachtowa Formation was as-
signed either to the Oravicum domain and pre-Late Albian
Magura Basin/Grajcarek Succession (see e.g. Birkenmajer
2007; Birkenmajer et al. 2008; Gedl 2008a) or exclusively to
the pre-Late Albian Magura Basin (e.g. Barski et al. 2012;
Oszczypko et al. 2012), structurally located either below the
overthrusted Pieniny-Subpieniny Nappes or in front of them
(see e.g. Birkenmajer 2007; Birkenmajer et al. 2008; Barski
et al. 2012; Oszczypko et al. 2012). Therefore, a critical
analysis of the Szlachtowa Formation in carefully described
sections is of high importance. Our analysis of similar de-
posits in central areas of the PKB (previously attributed to
the Oravic domain successions, Birkenmajer 1977) shows
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that the Bajocian deposits in the Podubocze section represent
the lowermost tectonic unit of the Pieniny Klippen Belt of
pre-Late Albian Magura Basin provenance (sensu Barski et
al. 2012). In this study, we focus on a succession of the
Szlachtowa Formation and younger deposits located at the
Sprzycne Creek at Dursztyn in the central part of the Pieniny
Klippen Belt in Poland (Fig. 1).
The dark turbiditic deposits cropping out along Sprzycne
Creek were originally attributed to the “Flysch Aalenian”
and placed in the Branisko Succession of the Pieniny
Klippen Basin by Birkenmajer (1958). Sikora (1971a) recog-
nized a thick succession of “black flysch” deposits with a
well distinguished bed of micaceous sandstone, a few meters
in thickness, in the upper part of this section. According to
Sikora (1971a), these deposits were stratigraphically over-
lain by the Sprzycne beds which are developed as light-grey
marly shales with intercalations of limestones and spotted
siderites. Higher, the Cenomanian Key Horizon represented
by green radiolarites is covered by variegated and green
shales with Upper Cretaceous microfauna (Sikora 1971a,c;
see Fig. 2 herein). Despite the lack of any biostratigraphic
markers (except for the uppermost member), the whole suc-
cession exposed at the Sprzycne Creek was assigned to a late
Early to Late Cretaceous age (Sikora 1971c) and attributed
to the Hulina Succession (synonymous with the Grajcarek
Succession). It is worth noting that the alleged equivalents of
the deposits described here were subsequently recognized
also in the eastern part of the Pieniny Klippen Belt in the
Małe Pieniny Mts – in the Grajcarek Succession, where
grey shales and marls of the Sprzycne Beds (Sikora 1971d;
see also Oszczypko et al. 2012) of Cretaceous age were dis-
tinguished directly above the so called Sztolnia Beds (in-
cluding the “black flysch” deposits). The Sprzycne Beds
were then treated as corresponding to the Opaleniec Forma-
tion of Birkenmajer (1977), and were also called the
Fig. 1. Position of the Pieniny Klippen Belt and Sprzycne Creek sec-
tion. 1 – sketch map with the position of the Pieniny Klippen Belt in
the Carpathians, 2 – tectonic map of the central sector of the Pieniny
Klippen Belt (modified from Książkiewicz 1972).
Opaleniec (Sprzycne) Formation by Oszczypko et al. (2012,
fig. 2). However, the age of the Opaleniec Formation re-
mained controversial. It was of Bajocian age according to
Birkenmajer et al. (2008) and of Albian—Cenomanian age ac-
cording to Oszczypko et al. (2012).
The timing of the first stratigraphic appearance and the
character of the deposits underlying the Szlachtowa Forma-
tion in the Pieniny Klippen Belt also remain enigmatic. The
slaty, marly “sub-flysch beds” originally placed below the
“black flysch” and assumed to be of Aalenian or Toarcian—
Aalenian age (Birkenmajer 1953) turned out to be in most
cases Cretaceous strata in tectonic contact with the former
(Birkenmajer & Pazdro 1963). In the other cases
(Birkenmajer & Pazdro 1963, fig. 5, bed 4c; Birkenmajer
1958), the “sub-flysch beds” yielded siderite nodules that are
characteristic of the Skrzypny Formation (Birkenmajer
1977). The Sprzycne Creek section provides an extended
record through both the base and top of the Szlachtowa For-
mation with a good biostratigraphic control.
Pieniny Klippen Belt
The Pieniny Klippen Belt predominantly consists of
marine sediments of the Oravicum domain (Mahet 1968)
(corresponding to the Pieniny Klippen Basin s.s.), in which
several bathymetric zones (successions or units) have been
distinguished, including the shallowest Czorsztyn Succes-
sion, the transitional Niedzica and Czertezik successions,
and the basinal Branisko-Kysuca and Pieniny successions
(Birkenmajer 1965; see also Mišík 1997). The depositional
environment was rather uniform across the basin during the
deposition of the monotonous marls and shales of the
Krempachy and Skrzypny formations during the Aalenian
(Birkenmajer 1977). The succession types of the Oravicum
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domain
acquired
their
identity during the latest
Aalenian or earliest Bajo-
cian when synsedimentary
tectonics led to the origin
of a submarine swell (Czor-
sztyn Ridge) (Fig. 3). The
Lower Bajocian is repre-
sented in the Oravicum ei-
ther by the deep-water
Harcygrund and Podzamcze
formations or hiatuses on
the elevations and their
slopes. The stratigraphy is
well-constrained by the
presence of ammonites in
either case (Myczyński
1973; Krobicki & Wierz-
bowski 2004).
At the same time, dark,
micaceous, turbidite se-
quences of the Szlachtowa
Formation were deposited
in the basin located to the
north of the Oravicum (see
Barski et al. 2012). The pa-
leogeographic position of
this region between the
Oravicum domain and the
North European Platform
during the early Middle Ju-
rassic is of essential impor-
tance in the current study.
We adopt here a term “pre-
Late Albian Magura Basin”
sensu Barski et al. (2012)
for this region, referring to
Fig. 2. Sikorais (1971a, fig. 40) original sketchy cross-section along middle Sprzycne Creek (see Fig. 4.1
for the approximate section line location); the original explanations given by Sikora 1971a, translated:
1 – cherty limestones – Jurassic—Neocomian, 2 – variegiated shales – Upper Cretaceous, 3 – Sztol-
nia Beds – Lower Cretaceous, 4 – Sprzycne Beds – Cenomanian, 5 – variegiated shales/Upper Creta-
ceous / +green shales with Mn-oxides coatings, 6 – tectonically brecciated black shales, 7 – Pomiedznik
Beds – Lower Cretaceous, 8 – variegiated marls and marly limestones /“Puchov Marls”/. x – thrust of
the Czorsztyn Unit.
Fig. 3. Idealized arrangement of facies zones and corresponding lithostratigraphic units of the Oravicum
domain and pre-Late Albian Magura Basin in the early Early Bajocian (modified from Barski et al. 2012).
some extent to the Mesozoic basement of the Magura Basin
of the Outer Carpathians. This term emphasizes the differ-
ence between the pre-Upper Albian (i.e. pre-orogenic) se-
quence and the uppermost Cretaceous—Paleogene flysch
cover. Although some authors advocate the unity and conti-
nuity of the Jurassic—Lower Cretaceous succession of what
is here called the pre-Late Albian Magura Basin and the
flysch succession of the Magura Basin s.s. (Birkenmajer
1977; Oszczypko 2004; Uchman et al. 2006), we separate
them as representing in fact two, completely different sub-
sidence/sedimentary regimes: the older one, terminated with
Scaglia Rossa-type redbeds, and the younger one, starting
with syn-orogenic Jarmuta-type clastics (regardless of their
continuous or discordant superposition).
We stress that the terms currently used for the sequences
comprising the Szlachtowa Formation, such as the Grajcarek
Succession (Birkenmajer 1977, 1986) or the Šariš Unit
(Plašienka & Mikuš 2010) are not synonymous with the
“pre-Late Albian Magura Basin”, because they do not define
the sedimentary basin as such, but rather refer to paleo-
tectonic units or sequences of strata corresponding to certain
parts of the basin.
Location and geological setting of the Sprzycne
Creek section
The uppermost tectonic unit at Dursztyn is represented by
the Pieniny Nappe, formed mainly by cherty maiolica-like
limestones and radiolarites of the Branisko Succession
(Fig. 4). The Jurassic/Lower Cretaceous klippen of the Czor-
sztyn Succession and their marly envelope occupy the adja-
cent zone to the north. The Sprzycne Creek section (analysed
in this study) is located still further to the north and is thus
tectonically below the Czorsztyn Succession; it represents
the paleogeographical area lying north of the Czorsztyn
zone. The northernmost chain of isolated rigid tectonic units
formed by red radiolarites and maiolica limestones (the con-
tact of the latter with the Kapuśnica Formation is visible
north of the site in the Sprzycne Creek cutting) has an un-
known structural affinity. It either represents a tectonic slice
(or syn-thrusting olistoliths) of the Pieniny Nappe or a facies
equivalent of the Branisko-Pieniny Succession in the pre-
Late Albian Magura Basin. The thick sequence of clastics
along the northern margin of the Klippen Belt (Jarmuta For-
mation) is a remnant of foreland sediments deposited during
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the Laramian thrusting of the Pieninic nappes (cf. Jurewicz
1997) and belongs to the flysch Magura Basin.
The Sprzycne Creek section is located geographically on
the northern slope of the Pieniny Spiskie range, 1.5 km
northeast of Dursztyn village (Figs. 1, 4). The deposits crop
out along the Sprzycne Creek over a distance of about 240 m
heading upstream. Coordinates of the beginning of the sec-
tion are: N 49°25’26.0”, E 020°12’19.0”. The approxi-
mately 200 m-thick succession is exposed in the stream bed
and the erosion escarpments. The lower half of the section is
poorly exposed, whereas the upper part is more continuous.
The beds are generally inclined steeply towards the south in
the lower and middle parts of the sequence (60—80°) but be-
Fig. 4. Geological situation of the Sprzycne Creek section. 1 – simplified bedrock map of the
area between Dursztyn and Frydman – see Fig. 1.2 for location, 2 – exposed intervals of strata
with sample locations.
come nearly vertical or even
somewhat overturned in the up-
per part. The Middle Jurassic
portion of the
Sprzycne Creek
section is mantled by variegiated
Cretaceous red and grey marls,
visible both at its base and top.
Material and methods
The chronostratigraphic posi-
tion of each sample from the
Sprzycne section was evaluated
on the basis of the reference
ranges of diagnostic dinoflagel-
late cysts, with notation of the
chronozones as defined after the
ammonite faunas according to
Callomon (1995), with the excep-
tion of the Jaworki Formation
that is barren of palynomorphs.
This study was focused on the
species most significant from a
stratigraphic point of view, while
the complete spectra of the di-
noflagellate cyst assemblages
will be published elsewhere. The
first (FAD) and last appearance
data (LAD) of selected dinofla-
gellate cyst species are extracted
from several references, prio-
ritized according to publication
date and paleogeographic affin-
ity with the northern Tethyan
margin. Some differences be-
tween the ranges of dinoflagel-
late cysts in the Pieniny/pre-Late
Albian Magura Basins, which
belonged to the Tethys Realm,
and the ranges recorded in epi-
platform areas of Europe should
be taken into account. The LAD-
based chronostratigraphic infer-
ences may also be affected by
redeposition. Twenty samples
were taken from the section: two samples represent the
Skrzypny-Szlachtowa Formation transition, ten samples rep-
resent the typical Szlachtowa Formation and eight samples
represent the Opaleniec Formation (Figs. 4, 5). Two other
samples were taken from the basis of the section: the lower-
most sample (SC-17) was picked from between two layers of
siderite concretions, while the second sample (SC-18) came
from above the micaceous sandstone bed, at a distance of
about 0.8 m above the first (Fig. 6.1). The sampling fre-
quency in the Szlachtowa Formation was higher in the top-
most, artificially exposed part of the formation (the interval
54—62 m on Fig. 5), up to the contact with the overlying
Opaleniec Formation. The lithologies of the samples consist
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of marls, shales and siltstones. The rock samples were pro-
cessed in compliance with standard palynological procedure
(Traverse 2007), which involved concentrated chloric and
fluoric acid treatment, wet sieving through a 15 µm nylon
mesh, and glycerin-jelly slide mounting. Thin-sections were
prepared to distinguish lithologically similar marly intervals
by means of microfacies. Planktonic foraminifera, which
were found only in the sections representing the Jaworki
Formation, provide some complementary stratigraphic data.
Results
Lithological succession and microfacies
The section starts with a few meters (not fully exposed) of
crumpled, slightly lustrous black shales with tabular sideritic
concretions up to ~ 20 cm in length (Fig. 6.1,3). This litho-
facies corresponds best to the Skrzypny Formation
(Birkenmajer 1977), with the exception of some beds a few
cm-thick of turbiditic micaceous sandstones/siltstones. It is
unclear whether such packets are of tectonic or sedimentary
character; in the first case they could be the slices of the
overlying Szlachtowa Formation, alternatively the described
interval as a whole can represent a sedimentary transition
from the topmost Skrzypny Formation into the Szlachtowa
Formation. The second eventuality, in the light of the strati-
graphic evidence (see below) seems to be reasonable and is
accepted herein.
Dark shales and siltstones alternating with sandstone tur-
bidites are characteristic of the central, thickest part of the
section (Fig. 5). These deposits with the appearance of
turbiditic beds, considering their lithological characteristics
given below, belong to the Szlachtowa Formation (cf.
Birkenmajer 1977). The proportion of shales and sandstones
varies upwards. The patchily exposed lower part of the unit
is mostly composed of shales with frequent but volumetri-
cally subordinate, up to 20 cm-thick sandstone layers. The
Fig. 5. Columnar lithological section of the upper part of the Szlachtowa Formation and the Opaleniec Formation in Sprzycne Creek at
Dursztyn, Pieniny Klippen Belt, Poland.
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first thicker ( ~ 1.3 m) bed of sandstone is exposed about half
way up the section. The lower 20 m of the relatively well ex-
posed topmost 60 m-thick interval of the Szlachtowa Forma-
tion consists of thick-bedded sandstones with rare shale
interbeds (Figs. 5, 6.4), while the overlying 40 m-thick inter-
val is generally shale-dominated (Figs. 5, 6.2), with sand-
stone beds not exceeding 0.4 m in thickness (except for the
interval 24.7—34 m, where massive sandstones prevail).
Graded, well-bedded sandstones to siltstones rich in mica
flakes are typical of the thin hard layers and they testify,
along with hieroglyphs (casts), that strata are not overturned.
Thick sandstone beds are often coarse-grained, brittle, and
poorly consolidated. They are weathered to almost the same
degree as the shale interbeds. They are also internally homo-
geneous and often synsedimentarily disturbed in the form of
large-scale bulbous load casts; they represent possible
fluxoturbidites. Abundant mica flakes impart a lamination to
the topmost parts of the sandstone-siltstone sets, and an ad-
mixture of crinoidal ossicles is common. The shales and
mudstones are also usually micaceous, black or grey in
colour, and they locally contain plant debris and thin coal
laminae. A few beds of allodapic crinoidal limestones (up to
0.3 m in thickness) and an interval with yellowish-grey spot-
ted marls occur in the artificially exposed uppermost eight
meters of the Szlachtowa Formation (Figs. 5, 7.3).
The contact of the Szlachtowa Formation with younger
deposits of the Opaleniec Formation is tectonic. It is marked
by calcitic veins and by a strong deformation of the sur-
rounding deposits. The top 8 m of the entire section consists
mostly of spotted marls and marly shales with a few thin in-
tercalations (0.01—0.1 m in thickness) of nodular spotted
limestones (Figs. 5, 7.1,4). These deposits can be subdivided
into two lithological types lying in a stratigraphic continuity:
a 5.5 m-thick interval of grey or greenish brittle marls, and
an about 2.5 m-thick interval of harder, slightly darker marly
shales with yellowish-brownish Fe/Mn coating. Marly lime-
stones show the microfacies dominated by filaments (Bositra)
(Fig. 8.1). The whole interval of the Jurassic spotted marls in
Sprzycne Creek thus represents the Opaleniec Formation in its
typical development (cf. Birkenmajer 1977). The contact with
the Cretaceous deposits is of tectonic character, marked by a
well developed, nearly vertical tectonic zone which stretches
approximately ENE—WSW along the stream (Fig. 7.2).
The Cretaceous deposits are represented by variegated, lo-
cally spotty, grey-green and red marly shales with subordi-
nate marly limestone intercalations (Scaglia Rossa-type
deposits). They are characterized by slightly silicified radio-
larian-foraminifera wackestone to mudstone microfacies
(Fig. 8.2—4). These deposits can probably be attributed to the
Jaworki Formation (of Birkenmajer 1977). They may corre-
spond to those from which Sikora (1971 a) reported the fora-
minifer Uvigerinammina jankoi Majzon. They are in tectonic
contact to the south with the deposits of the Czorsztyn Suc-
cession (Sikora 1971a; see Fig. 2 herein).
Biostratigraphy
Skrzypny Formation (topmost/transitional part)
The samples SC-17 and SC-18 contain very similar di-
noflagellate cyst assemblages characterized by high abun-
dance of Adreedinium elongatum ( = Phallocysta elongata).
Other stratigraphically meaningful species are represented
by Nannoceratopsis dictyambonis, Nannoceratopsis evae,
Pareodinia ceratophora and Dissiliodinium lichenoides
(Figs. 9, 10). The lower stratigraphic limit of P. ceratophora
Fig. 6. Lower and middle part of the Sprzycne Creek section (2014). 1, 3 – tectonic contact of the Jaworki Formation with the Skrzypny
Formation/transition to the Szlachtowa Formation (sid – siderite concretions, ms – micaceous sandstone bed); 2 – shale-dominated in-
terval of the Szlachtowa Formation ( ~ 2 m above sample SC-3); 4 – brittle sandstone-dominated interval of the Szlachtowa Formation;
white dots indicate sample locations.
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according to Riding & Thomas (1992) spans the undifferen-
tiated Middle Aalenian, but some detailed reports show its
later appearance in the Late Aalenian (Feist-Burkhardt 1990;
Riding et al. 1991) or earliest Bajocian (Riding 1987). This
species occurs already in the Late Aalenian of the Pieniny
Klippen Belt (Segit 2010). D. lichenoides, as well as Evansia
eschachensis recognized in sample SC-17, also do not occur
below the upper Middle Aalenian and Upper Aalenian, re-
Fig. 7. Uppermost part of the Sprzycne Creek section (2013/2014). 1 – general view from the stream scarp to NW and the position of the
2, 3 and 4; 2 – tectonic contact of the Opaleniec and Jaworki formations in the stream bed; 3 – artificially exposed topmost part of the
Szlachtowa Formation at the contact with the Opaleniec Formation; 4 – exposure of the Opaleniec Formation; panorama views 3 and 4 are
somewhat distorted, white dots indicate sample locations, hashed lines indicate tectonic disturbances. ct – crinoidal turbidite beds.
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spectively, either in the PKB or elsewhere (Feist-Burkhardt
& Monteil 2001). The upper stratigraphic limits of most of
the species mentioned above lie in the Laeviuscula or
Propinquans Zones of the Lower Bajocian; only the LAD of
N. evae is restricted to the Discites Zone of the lowermost
Bajocian (Prauss 1989). The absence of Scriniocassis
priscus (common in lower Aalenian and ranging up to the
Upper Aalenian in the PKB, Segit 2010), and Dissiliodinium
giganteum and Durotrigia daveyi (typical of the upper
Lower Bajocian, Fig. 9) is noteworthy. To conclude, the
most probable age of the topmost part of the Skrzypny For-
mation is the latest Late Aalenian or the earliest Early
Bajocian (late Concavum to Discites Zone).
Szlachtowa Formation
The sample SC-19 is almost the same as SC-17 and SC-18
with regard to its dinoflagellate cyst assemblage, with the
exception of relative abundance of individual species. De-
spite the general paucity of marine palynomorphs, most
samples of the Szlachtowa Formation from the Sprzycne
Creek section contain stratigraphically diagnostic repre-
sentatives of the Durotrigia, Dissiliodinium and Aldorfia
(Figs. 9, 10). Earlier studies have revealed these genera are
locally abundant at other sites exposing the Szlachtowa For-
mation (Segit 2010; Barski et al. 2012). Dissiliodinium
giganteum, which is a marker species for the Discites/
Laeviuscula—Propinquans zones of the Early Bajocian in
south-west Germany (Feist-Burkhardt & Wille 1992; Feist-
Burkhardt & Monteil 2001), occurs in samples SC-20, SC-1,
SC-2, and SC-5. The presence of Mancodinium semitabulatum
(providing its in-situ occurrence) restricts the top position of
sample SC-6 to the Humphriesianum Zone. Durotrigia
daveyi, with its lower limit in the Laeviuscula Zone and the
top in the Niortense Zone of the Late Bajocian (Feist-
Burkhardt & Wille 1992), occurs in samples SC-1, SC-2,
SC-3 and SC-9, while the Durotrigia occurs in all samples
except for SC-8 and SC-7. In the uppermost exposed beds of
the Szlachtowa Formation, D. daveyi co-occurs with Aldorfia
aldorfensis (sample SC-9). The topmost beds of the Szlach-
towa Formation exposed in the Sprzycne Creek section thus
can be attributed to the lowermost Upper Bajocian because
Fig. 8. Typical microfacies of the Middle Jurassic and Cretaceous marly deposits from the Sprzycne Creek section, Pieniny Klippen Belt,
Poland. 1 – filamentous (Bositra) packstone with quartz admixture (thin hard limestone bed with Fe-Mn coatings, upper part of the Opale-
niec Formation, Middle Jurassic); 2—4 – radiolarian/radiolarian-foraminifera wackstones, slightly silicified (Jaworki Formation, upper
Cretaceous); fot. 1 and 2 – crossed nicols. Scale bar applies to all micrographs.
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the FAD of A. aldorfensis is located in the Niortense Zone
(Feist-Burkhardt & Wille 1992).
Sample SC-7 contains a species and specimen-poor as-
semblage of exclusively long-ranging or stratigraphically
non-diagnostic taxa (such as Nannoceratopsis gracilis,
Kallosphaeridium praussii and Batiacasphaera sp.), while
sample SC-8 also contains Andreedinium elongatum
( = Phallocysta elongata) and rare Scriniocassis priscus.
These two latter species, otherwise abundant in the ammo-
nite-constrained Aalenian strata of the Skrzypny Formation
in the Pieniny Klippen Belt (Segit 2010) and, in the case of
A. elongatum, also common in the lowermost samples SC-17,
SC-18 and SC-19 of the Sprzycne section, could span the
Early Bajocian (Riding & Thomas 1992; Feist-Burkhardt &
Wille 1992). Assuming that the strata are tectonically not du-
plicated, the superposition of sample SC-8 above sample
SC-7 shows that both are in fact not older than the late Early
Bajocian (Fig. 9). This inference is also supported by the oc-
currence of rare Durotrigia sp. in sample SC-8. The Triassic
cysts of Rhaetogonyaulax rhaetica consistently present
throughout the section suggest that some Toarcian—Aalenian
sediments (where these cysts are encountered commonly)
were affected by synsedimentary redeposition and thus en-
riched the Bajocian strata with older cysts.
Dinocyst stratigraphy indicates that the sample SC-19
taken from the lowermost part of the Szlachtowa Formation
s.s. (above the transition from the topmost Skrzypny Forma-
tion; see Fig. 4.2), represents the upper Concavum Zone of
the Late Aalenian or the Discites Zone of the earliest Bajocian.
The interval between the samples SC-20 and SC-5 probably
represents the Laeviuscula and/or Propinquans zones of the
Early Bajocian, the dinocyst-poor sample SC-6 could reach
up to the Humphriesianum Zone, and the sample SC-9 corre-
sponds to the Niortense Zone of the Late Bajocian (Figs. 9,
13). Due to the paucity of dinoflagellate cysts and domi-
nance of long-ranging taxa, samples SC-7 and SC-8 can be
assigned to Laeviuscula—Niortense zones.
Opaleniec Formation
The dinoflagellate cyst assemblages in the lowermost part
of the Opaleniec Formation (Figs. 9, 11, 12) differ distinctly
from the underlying beds of the Szlachtowa Formation, fol-
lowing a slight tectonic displacement at the contact of the
units (Figs. 5, 7.4). The stratigraphically diagnostic species
that were encountered in sample SC-10 are Meiourogo-
nyaulax valensii (dominant in the assemblage) and the
Valensiella/Ellipsoidictyum plexus, both having their FAD
Fig. 9. Stratigraphic range chart compiled from: 1 – Feist-Burkhardt & Wille (1992), 2 – Feist-Burkhardt & Monteil (2001), 3 – Prauss
(1989), 4 – Burkhalter et al. 1997, 5 – Feist-Burkhardt & Monteil (1997), 6 – Riding & Thomas (1992), 7 – Feist-Burkhardt (1990),
8 – extended ranges observed in the PKB (Segit 2010), and distribution of the selected dinoflagellate cysts in the Sprzycne Creek section.
Approximate stratigraphic positions of samples are given (see also Fig. 13) (x – common to rare occurrence, + – very rare or single oc-
curence, some specimens may be redeposited).
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in the upper Humphriesianum Zone of the Early Bajocian.
Chytroeisphaeridia chytroeides has its FAD in the Niortense
Zone of the Late Bajocian (Feist-Burkhardt & Wille 1992;
Feist-Burkhardt & Monteil 1997). Early Meiourogonyaulax
Fig. 10. Dinoflagellate cysts from the Middle
Jurassic Skrzypny and Szlachtowa formations
of the Sprzycne Creek section, Pieniny Klippen
Belt, Poland. 1a,b – Durotrigia daveyi Bailey,
1987; sample SC-3; 2 – Evansia eschachensis
Below, 1990; sample SC-17; 3 – Pareodinia
ceratophora Deflandre, 1947; sample SC-17;
4 – Nannoceratopsis evae Prauss, 1989; sam-
ple SC-17; 5 – Nannoceratopsis dictyambonis
Riding, 1984a; sample SC-17; 6 – Dissiliodinium giganteum Feist-Burkhardt, 1990; sample SC-1; 7 – Dissiliodinium lichenoides Feist-
Burkhardt & Monteil, 2001; sample SC-17; 8, 9 – Aldorfia aldorfensis (Gocht, 1970) Stover & Evitt 1978; sample SC-9; 10, 11 – Anreedi-
nium elongatum (Beju, 1971) Feist-Burkhardt & Monteil in Feist-Burkhardt 1990; sample SC-17; 12 – Mancodinium semitabulatum
Morgenroth, 1970; sample SC-3. Scale bar applies to all photographs.
species (of which M. valensii is a representative) were re-
ported to be very common below the Early-Late Bajocian
boundary in southwest Germany (Feist-Burkhardt & Wille
1992). Sample SC-11 also yielded Endoscrinium asymmet-
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ricum (with its FAD in the Niortense Zone), and Ctenido-
dinium combazii, which has its lower limit in the Garantiana
Zone (Riding & Thomas 1992) or even the uppermost
Parkinsoni Zone of the Late Bajocian (Feist-Burkhardt &
Wille 1992). Species appearing at the base of the Upper
Bajocian, namely Ctenidodinium continuum, Carpatho-
dinium predae, Gonyaulacysta pectinigera and Atopodinium
polygonale, occur in sample SC-12. Cleistosphaeridium sp.
and Willeidinium bajocassinum (with FAD recorded in the
Parkinsoni Zone) occur in the section from sample SC-13
Fig. 11. Dinoflagellate cysts from the Middle Jurassic Opaleniec Formation of the Sprzycne Creek section, Pieniny Klippen Belt, Poland.
1 – Gonyaulacysta pectinigera (Gocht, 1970) Fensome 1979; sample SC-13; 2 – Endoscrinium asymmetricum Riding, 1987; sample SC-13;
3 – Atopodinium polygonale (Beju, 1983) Masure 1991; sample SC-15; 4 – Atopodinium cf. prostatum (Drugg, 1978) Masure 1991; sam-
ple SC-15; 5 – Cleistosphaeridium sp.; sample SC-15; 6 – Valensiella cf. ovulum (Deflandre, 1947) Eisenack 1963; sample SC-15;
7 – Chytroeisphaeridia chytroeides (Sarjeant, 1962) Davey 1979; sample SC-15; 8, 9 – Carpathodinium predae (Beju, 1971) Drugg
1978; sample SC-15; 10 – Tubotuberella dangeardii (Sarjeant, 1968) Sarjeant 1982; sample SC-14. Scale bar applies to all photographs.
upwards. Ctenidodinium cornigerum, also recognized in that
sample, has not been observed yet below the uppermost part
of the Parkinsoni Zone (Feist-Burkhardt & Monteil 1997) or
even Zigzag Zone (Riding & Thomas 1992; Poulsen 1998)
of the Upper Bajocian, while E. asymmetricum, on the other
hand, declined in the Zigzag Zone (Feist-Burkhardt & Wille
1992). Sample SC-14 yielded specimens of Adnato-
sphaeridium caulleryi and Tubotuberella dangeardii, with
FAD diagnostic of the Zigzag Zone (Riding & Thomas
1992; Feist-Burkhardt & Wille 1992) or Tenuiplicatus Zone
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Fig. 12. Dinoflagellate cysts from the Middle Jurassic Opaleniec Formation of the Sprzycne Creek section, Pieniny Klippen Belt, Poland.
1 – Adnatosphaeridium caulleryi (Deflandre, 1939) Williams & Downie 1969; sample SC-16; 2 – Ctenidodinium combazii Dupin, 1968;
sample SC-14; 3 – Ctenidodinium continuum Gocht, 1970; sample SC-14; 4 – Willeidinium bajocassinum Feist-Burkhardt, 1995; sample
SC-14; 5 – Ctenidodinium cornigerum (Valensi, 1953) Jan du Chęne et al. 1985; sample SC-14; 6, 7 – Meiourogonyaulax valensii Sarjeant,
1966b; sample SC-10. Scale bar applies to all photographs.
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of the Early Bathonian (in the case of A. caulleryi in Feist-
Burkhardt & Wille 1992). The stratigraphy of samples SC-15
and SC-16 is based on the co-occurrence of Carpathodinium
predae, Atopodinium prostatum and Willeidinium bajocas-
sinum. The upper limit of Carpathodinium predae usually
spans the Middle Bathonian Progracilis Zone (Riding & Tho-
mas 1992) or Morrisi Zone (Feist-Burkhardt & Wille 1992).
Although the FAD of A. prostatum was recorded in the
Tenuiplicatus Zone (Riding & Thomas 1992), while W.
bajocassinum, according to Feist-Burkhardt (1995) and Feist-
Burkhardt & Monteil (1997), has its LAD in the Zigzag Zone,
both species were listed by Poulsen (1998, fig. 3 therein) from
the Tenuiplicatus Zone in the Ore Bearing Częstochowa Clay
Formation in southern Poland (although W. bajocassinum is
very rare and was not illustrated). M. valensii with its LAD in
the Zigzag Zone implies that the sample SC-14 still belongs to
the lower Lower Bathonian.
The stratigraphy of the Opaleniec Formation is deduced
mainly on the basis of FADs; only a few species went extinct
in the Early Bathonian. To conclude, the diagnostic species
appear in the section of the Opaleniec Formation in a general
stratigraphic order that corresponds to the successive zones
of the Late Bajocian and Early Bathonian. Tectonics affects
the stratigraphic continuity of the transition from the
Szlachtowa Formation to the Opaleniec Formation only
weakly, leaving probably a stratigraphic gap that spans only
a part of the Niortense Zone. The samples can thus be as-
signed to the interval from the Niortense Zone of the Late
Bajocian up to the Zigzag or Tenuiplicatus Zones of the Early
Bathonian (Figs. 9, 13).
Jaworki Formation
No dinoflagellate cysts were found in the marly deposits
of the Jaworki Formation. The analyses of planktonic fora-
minifera carried out on thin sections (Dr. Zofia Dubicka,
pers. comm.) revealed some Upper Albian taxa in the grey-
greenish spotted marl samples taken from immediately
above the contact with the Opaleniec Formation and
Turonian taxa in the red marl samples taken a few meters
above the former (possible tectonic gaps occur between the
sampling points).
Fig. 13. Lithostratigraphic scheme of the Aalenian—Lower Bathonian (Middle Jurassic) of the Pieniny Klippen Belt (after Wierzbowski et
al. 2004; Segit 2010, modified). Stratigraphic positions of samples studied from the Sprzycne Creek section are shown; the arrowed inter-
vals indicate maximum possible range based on dinoflagellate cyst co-occurrences and superposition.
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Discussion
Stratigraphy of the turbidite succession (Szlachtowa For-
mation)
The deposits of the Szlachtowa Formation of Sprzycne
Creek contain dinoflagellate cyst assemblages characteristic
of the Late Aalenian or Early Bajocian to early Late Bajocian
age. The upper portion of the Szlachtowa Formation is prac-
tically of the same age as in sections studied previously at
Podubocze and Hałuszowa near Czorsztyn in the Pieniny
Klippen Belt (Barski et al. 2012) and consistent with some of
the stratigraphic assessments given by Gedl (2008a,b). How-
ever, the onset of turbidite sedimentation in the pre-Late
Albian Magura Basin and the character of the underlying
strata remains controversial.
The Lower Aalenian ammonites Leioceras opalinum and
Leioceras cf. comptum were described from the Szlachtowa
Formation in the Sztolnia creek section south of Szlachtowa
village (Birkenmajer & Myczyński 1977). Notwithstanding
the very poor state of preservation of this assemblage, as
well as the marked tectonic disturbance of the section and
the untypical lithology of the host rock (spotted limestones
resembling the Krempachy or Opaleniec formations rather
than the Szlachtowa Formation), the assumption about the
existence of Upper Toarcian—Lower Aalenian strata within
the Szlachtowa Formation deposits persisted (Birkenmajer
1977). Such a view suggesting that the deposition of the
Szlachtowa Formation started during the Toarcian was re-
peated also by Gedl (2008a, 2013) and Gedl & Józsa (2015).
According to Gedl (2008a, fig. 165), in addition to the up-
per Upper Aalenian and Bajocian, also the lower Upper
Toarcian is represented in the Szlachtowa Formation, whereas
the uppermost Toarcian to lower Upper Aalenian interval is
spanned by sedimentary hiatus. The Toarcian cyst-based ages,
however, were based on mostly poorly-preserved assemblages
consisting mostly of long-ranging and weakly-specific repre-
sentatives of Nannoceratopsis spp. and Kallosphaeridium
spp., to a total absence of taxa restricted to the Toarcian. There
are also no sedimentary indices of non-deposition in the
middle, or in any other parts of the Szlachtowa Formation.
The Toarcian age of the deposits of the Szlachtowa Formation
in the Podubocze section as proposed by Gedl (2008a) was
questioned by Barski et al. (2012), who proved the Bajocian
age of these strata based upon superposition. However, Gedl
(2013) recognized the presence of the Upper, Middle and
Lower Aalenian/?Upper Toarcian in the Szlachtowa Forma-
tion at the Szczawnica—Zabaniszcze section.
None of the dinoflagellate cyst taxa listed by Gedl (2013)
from the Szczawnica—Zabaniszcze section are strati-
graphically restricted to the Toarcian or Aalenian, whereas
Pareodinia sp. and Korystocysta sp. as reported by him from
the lowermost sample studied (allegedly representing the ?Up-
per Toarcian/Lower Aalenian; see Gedl 2013, fig. 14), have
not been reported elsewhere below the Middle Aalenian and
the Upper Bajocian, respectively (e.g. Riding & Thomas
1992). Considering the evident redeposition of Triassic
palynomorphs in the Bajocian strata of the Szlachtowa Forma-
tion, as shown here and in some previous studies (eg. Segit
2010; Barski et al. 2012), the possible presence of dinoflagel-
late cysts common in/or restricted to the Toarcian/Aalenian
should also be interpreted with caution.
The Middle—Late Toarcian age of a part of the Szlachtowa
Formation was recently postulated by Gedl & Józsa (2015),
who studied outcrops and a tectonically sliced borehole sec-
tion (Jar-1) at Jarabina and Kamienka in Eastern Slovakia.
The stratigraphic inferences of Gedl & Józsa (2015) are
partly based on the absence of some stratigraphically-
diagnostis species, namely the lack of dinoflagellate cysts
which were considered by them as Late Toarcian/Aalenian
indices, such as Nannoceratopsis dictyambonis, Phallocysta
elongata, Dissiliodinium spp. and Kallosphaeridium—Dissilio-
dinium plexus, in otherwise low-diversity assemblages com-
posed of Nannoceratopsis spp. (N. gracilis, N. raunsgaardii,
N. deflandrei, N. ambonis) and Kallosphaeridium spp. (Gedl
& Józsa 2015, pages 111—113). In our opinion, Nannoce-
ratopsis deflandrei, which was used as the only Toarcian
marker species in their study, can hardly be approved as a
key species in stratigraphy due to two reasons. Firstly, its
separation from morphologically diverse N. gracilis is disput-
able (Evitt 1962; Prauss 1989; see also Bucefalo-Palliani &
Riding 1997, fig. 9, table 1) and even if assumed, its distinc-
tive feature is subtle (i.e. fine ornamentation of the wall) and
can be obliterated to varying extents depending on preserva-
tion conditions. Secondly, the global upper stratigraphic limit
of Nannoceratopsis deflandrei s.l. does not correspond to the
Toarcian, but to the Callovian (N. deflandrei subs. senex – see
Bucefalo-Palliani & Riding 1997; Upper Bajocian/Batho-
nian in the case of N. deflandrei subs. deflandrei – see
Mantle & Riding 2012). In addition, the range base of the
Kallosphaeridium—Dissiliodinium combination (referred to
thin-walled, undeterminable representatives of these two gen-
era) was extended down to the Upper Toarcian by Gedl &
Józsa (2015, page 111), but FAD of Dissiliodinium sp. in fact
corresponds to the upper Middle Aalenian (Feist-Burkhardt &
Monteil 2001). The Middle Toarcian substage, according to
Gedl & Józsa (2015), is represented by only one sample re-
covered from borehole Jar-1 at a depth of 61.9 m, where
some poorly preserved, broken specimens of foraminifer
Lenticulina cf. chicheryi were identified. Apart from the in-
conclusive taxonomic determination implying uncertain strati-
graphic position of the sample, the core interval 61—79.5 m
is devoid of the sandstone intercalations typical of the
Szlachtowa Formation (see Birkenmajer 1977). Gedl & Józsa
(2015) also sampled a large exposure of the Szlachtowa For-
mation at Riečka Stream near Kamienka and ascribed it to
the Lower Bajocian (as also shown by Segit 2010 and Barski
et al. 2012). However, the overlying strata (their normal
stratigraphic position is ascertained by graded crinoidal
calciturbidites – Segit 2010), cropping out down the creek
in the dip direction and represented by samples Kmn4—8,
were surprisingly attributed to the Upper Toarcian and up-
per Middle—Upper Aalenian (Gedl & Józsa 2015, page 111,
fig. 17). Therefore, the above-mentioned doubts and objec-
tions seem to invalidate the position of the lower stratigraphic
limit of the Szlachtowa Formation as suggested by Gedl &
Józsa (2015). Considering preservational, sedimentological
and ecological variables controlling occurrence of particular
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dinoflagellate cyst species, as well as the unknown relation-
ship between species richness and number of specimens and
the discontinuity of studied sections, stratigraphic assessments
based on the absence of diagnostic dinoflagellate cyst species,
rather than on co-occurrence of found species, are not reliable.
Gedl 2013 (fig. 15b) and Gedl & Józsa 2015 (fig. 4k) pre-
sented the same field photograph of the fragmented ammonite
Brasilia (Brasilia) sp. found in the Szlachtowa Formation in
Eastern Slovakia (Jarabina). Although this ammonite clearly
supports the presence of at least Upper Aalenian strata in the
Szlachtowa Formation, we consider that this small and flat-
tened cast does not show ribbing features (on the basis of per-
sonal observation) that would be clear enough to distinguish
Middle from Upper Aalenian graphoceratid fauna with confi-
dence (i.e. Brasilia sp. vs. Graphoceras sp.).
Although strongly deformed by tectonics, the lower part of
the Sprzycne Creek section provides unique insights into the
character of the strata underlying the Szlachtowa Formation
which can be attributed to the Skrzypny Formation or the tran-
sitional beds. The siderite-bearing shales and the basal part of
turbidite sequence (represented by samples SC-17—SC-19) are
palynologically very similar and stratigraphically very close to
each other. Therefore, such similarity points to the original
sedimentary or just slightly disturbed position of the strata of
the Upper Aalenian and/or lowermost Lower Bajocian.
The superposition of the Skrzypny and Szlachtowa forma-
tions is reported for the first time in our study. Such superpo-
sition, although usually not immediately evident due to
tectonic complications, seems to be relatively common. We
observed it and examined it palynologically in the
Hałuszowa Stream section (just above the site described in
Barski et al. 2012), in the road cut north of the Chotuč Pass
at Vršatské Podhradie (Segit 2010), in the stream escarpment
south of the large exposure of the Skrzypny Formation at
Zázrivá in Western Slovakia (see Aubrecht et al. 2004; Segit
2010) and in the road cut near Udol (Ujak) in Eastern
Slovakia (see “sideritic limestone” and “marly shales and
sandstones” erroneously ascribed to the Cretaceous by
Oszczypko et al. 2004, fig. 4). If the sedimentary nature of
these contacts between formations is substantiated, the struc-
tural and paleogeographic position of each particular site and
their surroundings will change significantly.
Early Czorsztyn Ridge development
Major facies change took place in the shallower successions
of the Oravicum domain at the Aalenian/Bajocian boundary,
when black shales with sideritic concretions were replaced by
black to pale green shales with phosphatic nodules (Segit
2010) prior to the period of nondeposition spanning most of
the Early Bajocian (Krobicki & Wierzbowski 2004). There-
fore, the simultaneous facies turnover in the Oravicum domain
and pre-Late Albian Magura Basin can be accounted for by an
uplift of the asymmetrical submarine swell (Czorsztyn Ridge).
This uplift was probably spatially complex, thus the start and
termination of turbiditic facies could have been diachronic in
different parts of the basin; although unequivocal stratigraphic
evidence for such diachronity have not been presented so far.
The southern slope of the Czorsztyn Ridge was probably
gentle (as indicated by gradual downslope facies transition
and by absence of turbidites) while the northern slope was
probably steeper, exposing bedrock to a great depth and thus
sourcing turbidites of the Szlachtowa Formation (Barski et al.
2012; see also Birkenmajer 2007; Segit 2013). However,
some crinoidal turbidites also occur in the Oravicum domain
in some portions of the western sectors of the PKB in Western
Slovakia (Segit 2010, 2013; see also Aubrecht & Ožvoldová
1994). The total lack of data on depositional settings, sea-floor
topography or distance from the opposite (i.e. northern) mar-
gin of the pre-Late Albian Magura Basin led to us leaving this
area out of consideration for our simplified and coherent depo-
sitional model (see Fig. 3). However, tilt-block extension gen-
erating some bedrock-exposing, submarine scarps at the
southern margin of the basin (as presumed in the model)
match up well to synchronous synsedimentary tectonics that
brought about hiatuses, clastic admixture and variability in the
thickness of Bajocian crinoidal limestones in the adjacent
Czorsztyn facies zone. Furthermore, the stratigraphic occur-
rence of crinoidal turbidites in the Szlachtowa Formation is
congruent with the timing of crinoid proliferation in the
Oravicum domain (Wierzbowski et al. 2004; Krobicki &
Wierzbowski 2004).
The deposits of the Opaleniec Formation in Sprzycne
Creek yielded abundant markers of the Upper Bajocian to
Lower Bathonian interval. The disappearance of dark
turbiditic lithofacies, and the appearance of the non-
turbiditic deposits of the Opaleniec Formation in the Late
Bajocian corresponds well to the general subsidence of the
Czorsztyn Ridge, and the onset of the pelagic deposition in
the Oravicum domain (Wierzbowski et al. 1999; Gedl
2008a; see also Fig. 13 herein).
From a broader paleogeographic perspective, we stress that
facies changes at the Aalenian/Bajocian and Early/Late
Bajocian boundaries, associated with early tectonic evolution
of the Czorsztyn Ridge, coincide with episodes of the ‘mid-
Cimmerian tectonic event’ represented by unconformities,
hiatuses and facies changeover in the Tethyan/north Peri-
Tethyan realms and adjoining boreal areas, for example, in the
Iberian Basin (García-Frank et al. 2008), Paris Basin (Jacquin
et al. 1998), North Sea (Underhill & Partington 1994), basins
of the Caucasus (Saintot et al. 2006), Alborz & Kopet-Dagh
(Fürsich et al. 2009).
Structural position of deposits representing the pre-Late
Albian Magura Basin
The Szlachtowa Formation and overlying deposits of
Sprzycne Creek, as well as similar deposits occurring about
1.3 km towards the west in Żłobny Creek on the Sosnowa
Skała klippe, have been interpreted as belonging to the
Grajcarek Succession appearing below the overthrusted de-
posits of the Czorsztyn Succession (Sikora 1971b,c,d). It
should be remembered that the Szlachtowa Formation de-
posits of Sprzycne Creek, Żłobne Creek, as well as some
other localities at Dursztyn, were originally placed in the
Branisko Succession of the Oravicum domain by Birkenmajer
(1958). This interpretation is incorrect because the strati-
graphic position of these and the directly overlying deposits,
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such as the Opaleniec Formation, excludes their attribution
to the Branisko Succession, where the same stratigraphic in-
terval is represented by another lithofacies, attributed to the
Harcygrund, Podzamcze, Flaki, Smolegowa, Czorsztyn and
Sokolica formations (Fig. 13; cf. also Barski et al. 2012).
The Szlachtowa Formation and the overlying deposits of
Sprzycne Creek as well as the other deposits mentioned
above (Żłobny Creek), similar to those at Podubocze and
other sections described previously (Barski et al. 2012), are
comparable to those of the Grajcarek Succession in the east-
ern part of the Pieniny Klippen Belt in Poland. Gedl (2008a,
fig. 46) interpreted the deposits of Kręty Creek near
Dursztyn in a similar way. The attribution of the Szlachtowa
Formation as well as the overlying deposits to the Grajcarek
Succession changes markedly the tectonic interpretation of
this region. The deposits of this succession appear below the
overthrusted deposits of the Czorsztyn Succession in several
tectonic windows between Sprzycne Creek and Kręty Creek
near Dursztyn and Krempachy.
The structural and paleogeographic interpretation of these
deposits is consistent with the results of Jurewicz (1997),
Oszczypko et al. (2010), Plašienka & Mikuš (2010) and
Plašienka (2012) in the eastern part of the Pieniny Klippen
Belt. These authors recognized that the Pieniny Nappe (in-
cluding the Pieniny and Branisko/Kysuca successions) and
the Subpieniny Nappe (including the Czertezik, Niedzica,
and Czorsztyn successions) of Oravicum domain provenance
are thrust over the deposits of the Grajcarek Succession, cor-
responding to the pre-Late Albian Magura Basin. The latter
has been renamed as the Faklovka or the Šariš unit due to its
newly proposed tectonic interpretation.
Interpretation of the “Sprzycne beds”
The Sprzycne beds according to the original definition of
Sikora (1971a,b,c,d) corresponded to the light grey marly
shales with intercalations of limestones and spotted siderites
overlying the “black flysch” deposits (Sztolnia beds), and oc-
curring below the “Cenomanian Key Horizon” in Sprzycne
Creek. These deposits were attributed to the Albian—Ceno-
manian and correlated with the Opaleniec Formation by
Oszczypko et al. (2012). We show, however, that the “Sprzycne
beds” occurring at Sprzycne Creek (i.e. its type locality) ac-
tually represent a set of deposits composed of fragments of
different lithostratigraphic units placed in tectonic contact
and of different ages: the marly shales of the Upper Bajocian/
Bathonian age corresponding to the Opaleniec Formation, and
the marly shales with marly limestone intercalations (Jaworki
Formation). Therefore the term “Sprzycne beds” should not be
used as it is misleading in stratigraphic correlations.
Some details of the Sprzycne section as described herein
differ from those given by Sikora (1971a) – e.g. lack of the
“Cenomanian Key Horizon” which corresponds to the radio-
larite Hulina Formation of Birkenmajer (1977) of Albian—
Cenomanian age. These differences may be easily explained,
however, by the local appearance or disappearance of tecton-
ically reduced units due to changes in the flow of Sprzycne
Creek during the long period of time in observations from
early 1970’s up to 2014.
Conclusions
The Jurassic succession of Sprzycne Creek consists of
(1) the topmost part of the Skrzypny Formation or transitional
beds from Skrzypny Formation to the Szlachtowa Formation
representing the Upper Aalenian or the lowermost Bajocian,
(2) the Szlachtowa Formation (“black flysch”) representing
the Upper Aalenian or the lowermost Bajocian to lowermost
Upper Bajocian, and (3) the Opaleniec Formation representing
the Upper Bajocian and the Lower Bathonian. The Cretaceous
variegated marls are in tectonic contact with the latter. Thus,
the “Sprzycne beds” as originally distinguished in their type
section consist of at least two tectonically amalgamated units
of Middle Jurassic and Cretaceous age. This study provides
further evidence that the dark turbiditic deposits in the Pieniny
Klippen Belt, with very high mica content and crinoidal debris
admixture, is of Jurassic and not Cretaceous age. The dino-
flagellate cyst assemblages in the Sprzycne Creek section is
indicative of several successive zones of the ?latest Aalenian/
Bajocian and Lower Bathonian, with a total absence of Creta-
ceous species. Therefore, the composition of dinoflagellate
cyst assemblages contradicts the suggestion of redeposited
Jurassic palynomorphs in allegedly Cretaceous “black flysch”
deposits. In addition, the suggestion of the pre-Late Aalenian
age of the Szlachtowa Formation seems unsubstantiated as
well. We propose that the “sub-flysch beds”, which referred to
the strata underlying the Szlachtowa Formation, is a redundant
synonym of the Skrzypny Formation. Our results, as well as
reinterpreted earlier data, suggest uniform depositional condi-
tions of the Skrzypny Formation both in the Oravicum domain
and in the area to the north prior the Late Aalenian. The pre-
Late Albian Magura Basin evolved separately from the
Oravicum domain after the uplift of the Czorsztyn Ridge, as
subsequently witnessed by the onset of turbidite sedimenta-
tion restricted to the northern foot of the ridge and the remark-
able facies dissimilarity in the adjacent basins. Thus the
section in the Sprzycne Creek represents pre-Late Albian
Magura Basin deposits. These deposits are overthrust by the
Subpieniny and Pieniny Nappes consisting of the Czorsztyn
and Branisko successions, which resulted in the inferior tec-
tonic position of the pre-Late Albian Magura Basin within the
structure of the Pieniny Klippen Belt.
Acknowledgments: This research was supported by an inter-
nal Grant from the Institute of Geology (Faculty of Geology,
University of Warsaw) No. BST 160600/2. We are grateful
to Zofia Dubicka, PhD (Dept. of Palaeontology, Institute of
Geology, University of Warsaw) for planktonic foraminiferal
dating of samples. We wish to thank three reviewers for their
insightful feedback and dr. E. Jurewicz for fruitful discus-
sions on the topic of this paper. R. Nawrot is gratefully ac-
knowledged for help and fieldwork assistance.
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