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81
31st IAS Meeting of Sedimentolog y Kraków 2015
GUIDEBOOK
Renata Jach, Jacek Grabowski, Andrzej Gaździcki, Alfred Uchman
The inception, growth and demise
of a pelagic carbonate platform:
Jurassic and Lower Cretaceous of the Krížna Nappe
in the Western Tatra Mountains
Guide to eld trip A6 • 21–22 June 2015
31st IA S
Meeting of Sedimentology
Kraków, Poland • June 2015
INTERNATIONAL ASSOCIATION
OF SEDIMENTOLOGISTS
Guide to eld trip A6 (21-22 June 2015)
The inception, growth and demise
of a pelagic carbonate platform:
Jurassic and Lower Cretaceous
of the Krížna Nappe in the Western Tatra Mountains
Renata Jach1, Jacek Grabowski2, Andrzej Gaździcki3 and Alfred Uchman1
1Institute of Geological Sciences, Jagiellonian University, Kraków (renata.jach@uj.edu.pl, alfred.uchman@uj.edu.pl)
2Polish Geological Institute, National Research Institute, Warsaw (jgra@pgi.gov.pl)
3Institute of Paleobiology, Polish Academy of Sciences, Warsaw (gazdzick@twarda.pan.pl)
Jach, R., Grabowski, J., Gaździcki, A. & Uchman, A., 2015. e inception, growth and demise of a pelagic carbonate plat-
form: Jurassic and Lower Cretaceous of the Krížna Nappe in the Western Tatra Mountains. In: Haczewski, G. (ed.),
Guidebook for eld trips accompanying 31st IAS Meeting of Sedimentology held in Kraków on 23nd–25th of June 2015. Kraków,
pp. 75-102.
Guidebook is available online at: www.ing.uj.edu.pl/ims2015
Polskie Towarzystwo Geologiczne 2015, ISBN 978-83-942304-0-1
Route (Figs. 1, 2): From Kraków we drive south by
E77 to Rabka, then by road 958 to the village of Witów.
In Chochołowska Valley (Dolina Chochołowska), to the
exposures located near Huciska Glade (Polana Huciska).
First-day hike starts from Huciska Glade, than leads
through Huciański Klin ridge (stops A6.1–A6.4) and ends
in Lejowa Valley (Dolina Lejowa; stops A6.5, A6.6). is
all-day eastward traverse runs along unsigned trail through
forest, with some fairly demanding hiking at altitudes
900–1300 m. e relatively short loop walk of the second
day starts from Huciska Glade and leads up along Długa
Valley (Dolina Długa) to the Pośrednie ridge (stop A6.7).
e way back from the Pośrednie ridge is an easy downhill
walk along Kryta Valley (Dolina Kryta; stop A6.8.1–4).
Introduction to the trip
e Tatra Mountains are the highest ridge of the West-
ern Carpathians with the highest peak Gerlach (2655 m).
e Tatra Mts were uplied during Neogene and form
a block which is asymmetrically tilted to the north and
bounded from the south by a prominent fault (Fig. 3).
Fig. 1. Route map of eld trip A6.
e block consists of a pre-Mesozoic crystalline
core (granitoidic intrusions and older metamorphic
rocks), ?Permian and Mesozoic autochthonous sedimen-
tary cover, allochthonous Mesozoic sedimentary rocks,
detached locally from their crystalline basement in form
of nappes and smaller thrust sheets (Kotański, 1965,
76
A6 — Inception, growth and demise of a pelagic carbonate platform
1971). e nappes were formed in Late Cretaceous. e
Mesozoic sedimentary rocks are discordantly covered
by rocks of the Central Carpathian Paleogene, which
include Oligocene ysch, more than 2 000 m thick, in
their upper part. e sedimentary rocks of the Tatra
Mts dip generally to the north due to the Neogene upli
(Fig. 4; Bac-Moszaszwili et al., 1979). ey are ascribed
to three main tectonic-facies domains: Tatricum (High-
Tatric autochthon and allochthon), Fatricum (Krížna
Nappe = Lower Sub-Tatric Nappe) and Hronicum (Choč
Nappe = Upper Sub-Tatric Nappe) on the basis of their
characteristic facies successions and tectonic position.
e Krížna Nappe overlies the High-Tatric units
and is covered by the Choč Nappe (Kotański, 1965). It
comprises Lower Triassic to Lower Cretaceous deposits
and is built of several thrust sheets and so called ‘partial
nappes’. e Krížna Nappe belongs to the Fatricum
Domain of the Central Carpathian block (Plašienka,
2012). During most of the Jurassic time, it was one of the
domains located between the Alpine Tethys to the north
and the Meliata Ocean to the south (Fig. 5; ierry and
Barrier, 2000; Schmid et al., 2008). As a consequence of
its location, the succession studied displays a strong simi-
larity to the Jurassic of other Tethyan basins.
During the Jurassic, the Fatricum Domain was
bordered by the uplied Tatricum Domain to the north
and the Veporicum and Hronicum domains to the south
(Csontos and Vörös, 2004; Plašienka, 2012). e Fatri-
cum Domain was regarded as being an extensional basin
during the Jurassic, located on thinned continental crust
(e.g., Plašienka, 2012). As a result, the Jurassic successions
of the Fatricum Domain are characterized by an almost
Fig. 2. Detailed itinerary of eld trip A.6; A6.1–4 - Huciański Klin ridge; A6.5–6 - Huty Lejowe glade; stops:A6.7–8a–c – Długa Valley and
Kryta Valley.
Fig. 3. Tectonic sketch map of the Tatra Mts showing location of the excursion area (aer Bac-Moszaszwili et al,. 1979; modied)
77
31st IAS Meeting of Sedimentolog y Kraków 2015
continuous record of deepening, with a transition from
littoral through hemipelagic to pelagic deep-sea sedi-
mentation.
e Jurassic deposits of the Krížna Nappe in the Tatra
Mts represent a generally deeper sea succession of the
Zliechov type (Michalík, 2007; Plašienka, 2012; Jach et
al., 2014). e oldest Jurassic deposits are represented
by dark shelf carbonates and shales, which refer to sea
transgression onto emerged lands (Figs 6–8; Gaździcki
et al., 1979; Michalík, 2007). ese Rhaetian–Hettang-
ian deposits have diachronic lower and upper bound-
ary. e Early Jurassic basin featured wide basins and
narrow horsts, characteristic of the rst phase of exten-
sion (Plašienka, 2012). e second phase of extension
took place during the latest Early Jurassic and resulted
in extensional tilting of blocks, which formed a horst-
and-graben topography (Wieczorek, 1990; Gradziński
et al., 2004; Jach, 2005; Plašienka, 2012). e formation
of horsts (e.g., the excursion area) and grabens (in the
High Tatra and the Belianske Tatry Mountains) led to
distinct facies changes (Guzik, 1959; Jach, 2007). e
subsiding basins were lled with Fleckenmergel-type
sediments (bioturbated “spotted” limestones and marls,
ranging from Sinemurian to Bajocian; Wieczorek, 1995;
Iwańczuk et al., 2013). During the Late Pliensbachian–
?Aalenian, the horsts acted as submarine highs with sedi-
mentation of spiculites on their slopes (Jach, 2002a) and
neritic crinoidal sedimentation (e.g., crinoidal tempes-
tites; Jach, 2005), replaced by condensed pelagic carbon-
ates (Gradziński et al., 2004) that were deposited on a
pelagic carbonate platform (sensu Santantonio, 1993).
During the Middle Jurassic, signicant topographic
relief was still present and controlled facies distribution.
e deposition of carbonate sediments terminated with
the onset of a uniform radiolarite sedimentation during
the Middle Jurassic (Jach et al., 2012, 2014). Generally,
the Lower–Upper Jurassic sediments of the Fatricum
Domain record a gradual deepening and transition
Fig. 4. Geological cross section through the Tatra Mts along the Dolina Kościeliska valley (aer Kotański, 1965, changed)
78
A6 — Inception, growth and demise of a pelagic carbonate platform
from hemipelagic to pelagic deep sea environment.
A major recovery of carbonate sedimentation started
in the Late Tithonian and Early Berriasian, when the
Maiolica-like deep sea limestones and marls were depos-
ited (Pszczółkowski, 1996; Grabowski et al., 2013). Wide-
spread marl and marly limestone sedimentation started
in the Late Berriasian and continued to the Aptian,
with intercalations of turbiditic sandstones and calcare-
ous uxoturbidites in the Valanginian and Hauterivian
(Pszczółkowski, 2003a).
e main aim of this excursion is to present general
depositional history of the studied part of the Krížna
Unit and to discuss factors controlling their sedimentary
environment.
Stop descriptions
Attention: All the localities are in the protected area
of the Tatra National Park. Please do not hammer the
rocks.
A6.1 Huciański Klin ridge
– Late Pliensbachian spiculites
(49°15´37˝ N, 19°49´17˝ E)
Leader: Renata Jach
e section presented during the rst part of the
excursion is located on the forested southern slope of the
Huciański Klin ridge. e oldest are 16–20 m thick spicu-
lites which overlie basinal “spotted” limestones and marls
of the Sinemurian–Lower Pliensbachian not exposed in
the presented locality (about 150 m thick; see stop A6.6).
Spiculites are well-exposed in crags a few metre high.
Late Pliensbachian age is ascribed to the spiculites on
the basis of their position in the section. ey are dark,
very hard and well-bedded, with bed thickness from
a few to 30 cm. Siliceous sponge spicules, which belong
to Hexactinellida and Demospongia (mainly Tetractinel-
lida) with loose skeletons, are the major components of
spiculites (Fig. 9A–C; Jach, 2002a). A gradual substitu-
tion of Hexactinellida by Demospongia is observed
Fig. 5. General palaeogeographic position of the Fatricum Domain during the Callovian (aer ierry and Barrier, 2000; simplied)
79
31st IAS Meeting of Sedimentolog y Kraków 2015
upward the spiculite section. Crinoidal ossicles, benthic
foraminifera and detrital quartz grains have also been
found in very small quantities.
Spiculites are interbedded with some crinoidal
wackestones, packstones and grainstones, which form
beds up to 20 cm thick. Limestone beds thicken upwards
and show a general trend of grain coarsening, accom-
panied by an increase in their textural maturity from
wackestones to grainstones (Jach, 2005). Low-angle
cross-bedding, normal grading and erosional bases
Fig. 6. Simplied litostratigraphic scheme of the Fatricum domain succession in the Tatra Mts (partly aer Lefeld et al. (1985); modied)
observed in crinoidal interbeds indicate that they are laid
down in higher energy conditions than the intervening
spiculites. is is attributed to the currents generated
by storms that were capable of sweeping crinoidal mate-
rial from shallow, elevated parts of the basin to the area
inhabited by siliceous sponges. As such, they represent
event beds deposited below storm wave base on the slopes
of an elevation. e gradual replacement of Hexactinel-
lida by Demospongia and grain coarsening and thicken-
ing of crinoidal intercalations indicate a shallowing trend
80
A6 — Inception, growth and demise of a pelagic carbonate platform
Fig. 7. Lithostratigraphic log of the Lower Jurassic–Early Cretaceous of the Krížna
Nappe in the Western Tatra Mts (aer Lefeld et al 1985; modied)
Fig. 8. Early–Middle Jurassic evolution of the studied part of the Fatricum Basin
(aer Jach, 2003; modied)
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31st IAS Meeting of Sedimentolog y Kraków 2015
during spiculite deposition (Jach, 2002a). Most probably
this trend was related to local changes of seaoor topog-
raphy caused by synsedimentary faulting in the Fatricum
Basin (Jach, 2005). is notion is supported by the occur-
rence of packages displaying chaotic bedding within the
spiculites in the upper part of the spiculite succession.
ey are interpreted as submarine slumps.
A6.2 Huciański Klin ridge – Early
Toarcian crinoidal limestones
(49°15´36˝ N, 19°49´21˝ E)
Leader: Renata Jach
White, grey and slightly pinkish crinoidal limestones
(grainstones) overlie spiculites. ey crop out directly over
spiculites in rock crags. e crinoidal grainstones, about
12 m in thickness, display irregular bedding with subtle
cross-bedding, graded bedding and erosional bed amal-
gamation. Crinoid stem plates (columnals) are predomi-
nant components whereas cirri and arm fragments are
less common (Fig. 9D; Głuchowski, 1987). Crinoid
assemblage is dominated by Isocrinus sp., Balanocrinus
sp. while Cyrtocrinida occur less commonly (Świńska
Turnia crag; Głuchowski, 1987). Fragments of echinoid
spines, mollusc and brachiopod shells, ostracods, bryo-
zoans, belemnite rostra, and benthic foraminifera occur
subordinately (Jach, 2005). An indistinct trend in coars-
ening of the crinoidal grains from 0.5 mm to 1–1.2 mm is
observed upward the sections.
A lack of stratigraphically diagnostic fossils hindered
the precise age determination of the crinoidal lime-
stones. ey are ascribed to the Lower Toarcian since
they are overlaid by red limestones of the latest Early–
Late Toarcian (Lefeld et al., 1985; Myczyński and Lefeld,
2003; Myczyński and Jach, 2009; see stop A6.4). Chem-
ostratigraphic data from crinoidal limestone indicate
that in their uppermost part a signicant δ13C positive
excursion occurs (δ13C ~ 3.6‰; Krajewski et al., 2001).
According to Jenkyns (2003), pronounced positive δ13C
excursion is associated with Early Toarcian Tenuicos-
tatum and Falciferum zones; the excursion is interrupted
with the negative shi in the early Exaratum subzone of
the Falciferum Zone. As the isotope excursion occurs
in the upper part of the crinoidal grainstones, it can be
assumed that this part of the section refers most probably
to the Tenuicostatum Zone of the Early Toarcian.
Fig. 9. Spiculites and crinoidal limestones. A) Spiculite in thin section. Plane-polarised light; B) Spiculite in thin section. Cross-polarised
light; C) Densely packed siliceous sponge spicules. SEM image of HF-etched surface; D) Crinoidal grainstone with syntaxial cements. in
section, plane-polarised light.
82
A6 — Inception, growth and demise of a pelagic carbonate platform
All the above described sedimentological character-
istics point to a multiple reworking and winnowing of
crinoidal material by storm-induced oscillatory currents
from elevated parts of the basin. us, the sedimenta-
tion of the crinoidal grainstones took place between
the storm and fair-weather wave bases. e succession
of the crinoidal intercalations in the spiculites and the
overlying crinoidal grainstones show a vertical transition
from distal to proximal tempestites, which is a record of
a progressive shallowing upward trend (Jach, 2005).
A6.3 Huciański Klin ridge – Early
Toarcian manganese deposits
(49°15´37˝ N, 19°49´20˝ E)
Leader: Renata Jach
e Mn-bearing deposits of the Krížna Unit in the
Western Tatra Mts occur locally between the crinoidal
tempestites (Lower Toarcian) and the pelagic red lime-
stones (Lower Toarcian−?Aalenian). ey crop out exclu-
sively between the Chochołowska and Lejowa valleys
where they were mined as Mn ore in the 19th century
(Jach, 2002b). e Mn-bearing deposits form a lens
which is up to 2 m thick and stretches at the distance of a
few hundred metres at the Huciański Klin ridge. e old
shas provide the only accessible outcrops of these rocks
there. e longest of them is 41 m long (Jach, 2002b). e
Falciferum Zone of the Early Toarcian may be estimated
for the Mn-bearing deposits on the basis of their posi-
tion in the section (Krajewski et al., 2001; Myczyński and
Lefeld, 2003; Myczyński and Jach, 2009).
For the purpose of simplicity, the Mn-bearing depos-simplicity, the Mn-bearing depos-
its are subdivided in three parts: rocks underlying the
Mn-rich bed (30–70 cm thick), the Mn-rich bed (up to
110 cm thick), and rocks overlying the Mn-rich bed (up
to 40 cm thick; Jach and Dudek, 2005; Fig. 10).
Generally rocks underlying the Mn-rich bed consist
of: (i) a Fe-rich layer, (ii) an X-ray amorphous Mn-oxide
layer, (iii) shales, and (iv) a massive jasper bed. e 15 cm
thick Fe-rich layer comprises up to ~30 wt% Fe (mainly
hematite). e overlying 10 cm thick Mn-oxide layer is
composed mainly of X-ray amorphous Mn oxide (up to
46 wt% Mn). Some 2–15 cm thick shales occur between
the rocks described above and the main Mn-rich bed.
Clay minerals comprise a complex suite dominated by
mixed-layer clays with chlorite, smectite, and vermicu-
lite layers (Dudek and Jach, 2006). e Fe-rich layer, and
the Mn-oxide layer underwent locally silicication which
resulted in the development of a massive jasper bed,
which is 10 to 50 cm thick (Figs 10, 11A, B).
e Mn-rich bed, with sharp and well dened top
and bottom, ranges in thickness from 35 cm to 1.1 m.
It comprises clearly dened, lenticular zones composed
either of Mn carbonates or of Mn silicates (Fig. 11C–E).
e carbonate zones are purple-red, whereas the silicate
zones are usually black.
e Mn-carbonate zones are built of calcite and
Mn-calcite, with various Ca/Mn ratios whereas Mn sili-
Fig. 10. Manganese-bearing deposits cropping out in a sha entrance. Lithological section with general geochemical characteristic (Si, Fe
and Mn).
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31st IAS Meeting of Sedimentolog y Kraków 2015
cates (braunite, caryopilite) occur in minor amounts
(Korczyńska-Oszacka, 1978; Jach and Dudek, 2005).
Pure rhodochrosite forms small lenses up to 6 cm long
in the upper part of the bed (Korczyńska-Oszacka, 1979).
Conversely, the silicate zones are dominated by braunite,
forming frequently idiomorphic crystals (Fig. 11F), and
caryopilite. Calcite and subordinate amounts of dolomite,
apatite, and barite have been identied as non-manganese
minerals. e chemistry of the carbonate and silicate zones
diers mainly in the Mn content: ~5 wt% Mn in the former
ones in contrast to more than ~50 wt% Mn in the latter
ones (Jach and Dudek, 2005). e Mn-rich bed comprises
low concentrations of transitional elements (Co + Ni + Cu
< 0.01 wt%). On a ternary diagram of Co+Ni+Cu, versus
Fe and Mn, our samples plot in the area of Mn deposits
of hydrothermal and diagenetic origins. In contrast, it is
enriched in Ba (up to 4500 ppm). Total REE (8 elements)
contents range from 83 to 151 ppm which may indicate
Fig. 11. Manganese-bearing deposits A) Jasper, polished slab; B) Internal structure of jasper bed, brous chalcedony and blocky quartz.
in section, cross-polarised light; C) Mn-bearing bed shows subtle stratication underlined by occurrence of carbonate and silicate zones.
Polished slab; D) Carbonate zone. Manganese oncoide within echinoderm grainstone, mainly echinoid-crinoidal, with syntaxial cements
built of calcite and manganese calcite. in section, plane polarised light; E) Silicate zone with abundant microbial structures, mainly
oncoids. in section, plane polarised light; F) Silicate zone. Authigenic idiomorphic crystals of braunite, SEM image of HCl-etched surface.
84
A6 — Inception, growth and demise of a pelagic carbonate platform
that the deposits studied may have formed by both
hydrothermal and hydrogenetic processes.
e Mn-rich bed, especially the silicate zones,
abounds in microbial structures: crusts and oncoids (Fig.
11C, E; Jach and Dudek, 2005). Crusts cover and bind
bioclasts. Oncoids, 3–30 mm across, are usually elongat-
ed, rarely isometric. e nuclei of the oncoids are usually
composed of bio- and lithoclasts, less frequently of barite
crystals (cf. Krajewski and Myszka, 1958). eir cortex
is composed of concentric laminae of Mn-silicates and
Mn-calcite. Microbial structures are accompanied by
bioclasts, namely fragments of echinoids and crinoids.
Tests of benthic foraminifera, shells of molluscs, ostra-
cods, holothurian sclerites, and bryozoan fragments
are less common. is assemblage of fauna and micro-
bial structures occurs exclusively within the Mn-rich
sequence; it is not found in the overlying or underlying
deposits or in deposits that are lateral equivalents of the
Mn-rich sequence.
Rocks overlying the Mn-rich bed are composed
of two layers of shale separated by a layer of bioclastic
limestone. e agglutinating foraminifera, represented
almost exclusively by Recurvoides, occur in the upper
shale (Tyszka et al., 2010). e clay fraction of the shales
is dominated by illite and illite-rich illite-smectite mixed-
layer clays (Dudek and Jach, 2006).
e Mn-bearing deposits are interpreted as formed in
several stages controlled by a pulse-like activity of a shal-
low submarine exhalative vent (Krajewski and Myszka,
1958; Jach and Dudek, 2005). It is proved by sedimento-
logical, mineralogical and geochemical evidence, coupled
with the occurrence of specic microbial structures and
a peculiar fauna assemblage (Jach and Dudek, 2005). e
limited lateral extent of the Mn-bearing sequence may be
an eect of low eciency of the vent and/or of the sea-
oor topography. e specic faunal assemblage domi-
nated by deposit feeders was intimately associated with
trophic conditions which persisted near the vent orice.
During cessation in the vent activity, the sediments
would have been exposed to and would have interacted
with sea-water. Other early diagenetic processes included
silicication and reduction of Mn oxides during suboxic
diagenesis (Krajewski et al., 2001). Hydrothermal activity
was the most likely source of colloidal silica. Idiomor-
phic shapes of braunite crystals embedded in Mn-calcite
indicate that silicication preceded crystallization of Mn
carbonates. e process of silicication resulted in the
formation of Mn silicates in the Mn-rich bed, the massive
jasper bed in the lower part of the sequence, and possibly
also numerous silica lenses in the underlying crinoidal
grainstones. e following stage of diagenesis – precipi-
tation of Mn carbonate cements in the Mn-rich bed, was
controlled by abundance of organic matter in the sedi-
ments. e latter is interpreted as genetically related to
the microbial productivity in situ.
e position of the Mn-bearing deposits over the
crinoidal tempestites and below the red pelagic lime-
stone indicates that they were laid down at neritic depths.
Moreover, it implies that Mn-bearing deposits mark a
substantial change from relatively shallow (tempestites)
to deeper water (red pelagic limestones) sedimentation
milieu. is change most probably resulted from synsed-
imentary tectonic activity. It is in line with expelling
of uids by the vent. It was associated with extensional
faults which provided channelways for geouid migra-
tion upward (Jach and Dudek, 2005). e internal facies
variation of the Mn-bearing sequence may be explained
by changes in bottom-water chemistry, geouid tempera-
ture or by lateral migration of the vent orices.
A6.4 Huciański Klin ridge – Lower
Toarcian-?Aalenian red limestones
and marlstones and Bathonian Bositra
limestones
(49°15´37˝ N, 19°49´24˝ E)
Leaders: Alfred Uchman, Renata Jach
e Mn-bearing sequence is covered by red lime-
stones and marlstones, about 4 m thick, which in turn,
are overlain by thin-shelled bivalve-bearing limestones
(hereaer called Bositra limestones). e latter are up to 3
m thick (Figs 12, 13A; Jach, 2007). e ammonites found
in the red limestones indicate the upper part of Lower
Toarcian–Upper Toarcian (Serpentinum–Pseudoradiosa
zones; Myczyński and Jach, 2009). e outcrop of red
limestones is located at the entrance to one of the Mn
adits.
e red limestones and marlstones are characterized
by concentrations of pelagic fauna remains (Fig. 13B),
such as ammonites, belemnites and sh teeth, which
are a common feature of the Jurassic pelagic limestones
deposited on elevated settings (pelagic carbonate plat-
85
31st IAS Meeting of Sedimentolog y Kraków 2015
forms sensu Sanantonio, 1993). Six microfacies have been
distinguished within red nodular limestones: crinoi-
dal-ostracod packstone, crinoidal packstone, crinoidal
wackestone, marly mudstone, Bositra packstone and
Bositra-crinoidal packstone (Gradziński et al., 2004).
Finning-upward trend (from packstones to wackestones),
is accompanied by increasing upward abundance of
microborings.
Crinoid and echinoid fragments are most abun-
dant within microfossil assemblage. Fish teeth, benthic
foraminifera, smooth-walled ostracods, juvenile ammo-
nites are less common (Gradziński et al., 2004). Echinoid
fragments dominate in the lower part of the red nodular
limestone section and decrease upwards. Conversely, sh
teeth are relatively rare in the lower part of the section
and abundant in the upper part.
e upper part of red limestones and marlstones
displays several features, such as concentration of
nektonic fauna remains, occurrence of stromatolites
and oncoids, and abundance of microborings typical of
condensed section deposited on submarine elevations
(Fig. 13A–D; Jenkyns, 1971; Bernoulli and Jenkyns,
1974). e features mentioned above collectively indicate
a low depositional rate.
Microbial-foraminiferal oncoids, which have been
recognized in the upper part of the red deposits, are the
most peculiar feature of the studied section (Fig. 13C,
D; Gradziński et al., 2004). e oncoids are up to 10 cm
across and mostly display discoidal shape. Intraclasts
or internal moulds of ammonites have acted as oncoid
nuclei whereas oncoid cortices are composed of dark red
laminae (mainly of iron hydrooxides/oxides), encrust-
ing foraminifera (Fig. 13D; Nubecularia a. mazoviensis,
Dolosella, and agglutinated Tolypammina) and calcite
cements. e dark red laminae dominate the oncoidal
cortices and show a reticulate ultrastructure which is
interpreted as mineralized biolm, visible under SEM.
Mineralized microbial bodies, globular and lamentous
in shape, also built of iron hydrooxides/oxides, are abun-
dant within the laminae. e association of foraminif-
era with microbes is supposed to be an adaptation of
foraminifera to oligotrophic condition on the sea oor.
It is very probable that biolms served as food source
for encrusting foraminifera. Formation of oncoids was
possible under periodic water agitation (Gradziński et
al., 2004).
e red limestones locally display nodular structure
and contain a few discontinuity surfaces in the studied
section (Gradziński et al., 2004). Some of such surfaces
are burrowed with alassinoides, which indicates
colonization of a rmground by crustaceans. Another
discontinuity surface, which occurs in the uppermost
part of the section, is manifested by concentration of
internal moulds of ammonites and some fragments
Fig. 12. Lithological section of the red limestones in the Huciański
Klin site (Gradziński et al., 2004)
86
A6 — Inception, growth and demise of a pelagic carbonate platform
of ammonite shells covered with a stromatolite (Fig. 13B).
ere is a concentration of glaucony grains and crusts in
the topmost part of the section, just at the contact of the
red limestones and the Bositra limestones.
Overlying Bositra limestones are composed of Bosi-
tra-crinoidal packstones, and Bositra packstones/grain-
stones in this section (Jach, 2007). e latter dominate in
the uppermost 3 m of the section. ey were laid down
in a relatively high-energy setting, which controlled the
good sorting of these deposits. However, the domination
of the Bositra bivalves seems to have resulted from some
ecological factors, such as eutrophication of the water
column. e dissolution of non-calcitic bioclasts is also
suggested. Bositra-limestones lack of index fossils; their
age is inferred as Lower Bathonian, based on superposi-Lower Bathonian, based on superposi-
tion (Jach et al., 2014).
e red nodular limestones and the overlying Bosi-
tra limestones were formed during gradual deepening
of the basin, which caused lowering of the depositional
rate and, hence, condensation (Wieczorek, 2001). e
deposition of Bositra limestones marks the rst stage of
unication of facies, which probably took place during
Lower Bathonian. is process was later manifested by
the deposition of radiolarites in the whole Fatricum
Basin (Ožvoldová, 1997; Polák et al., 1998; Jach et al.,
2012, 2014). us, the deposition of Bositra limestones
reected the intermediate stage in the basin evolution
leading to formation of radiolarites (Lefeld, 1974; Jach,
2007).
A6.5 Lejowa Valley – Lower Jurassic
mixed siliciclastic/carbonate deposits
(49°15´46˝ N, 19°50´39˝ E)
Leader: Andrzej Gaździcki
e uppermost Triassic and lowermost Jurassic
strata of the Fatricum (Krížna Nappe) in the Tatra Mts
are represented by marly shales and quartz sandstones
with limestone intercalations (Uhlig, 1897; Goetel,
1917; Gaździcki, 1974, 1975, 1983, 2003, 2014; Uchman,
Fig. 13. Red limestones. A) Section of the red limestones and Bositra limestones at the entrance to one of the adits; B) Omission surface
with ferruginous stromatolite encrusting ammonite mould and shell (Lytoceras sp.). Weathered surface; reprinted from Myczyński and Jach
(2009); C) Cross-section through a microbial-foraminiferal ferrugineous macrooncoids. Polished slab; D) Cortex of oncoid built of encrust-
ing foraminifers; thin section, plane-polarised light.
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31st IAS Meeting of Sedimentolog y Kraków 2015
1991; Krobicki and Uchman, 1993; Hołda, 2002). ey
are assigned to the Fatra and Kopieniec formations
(Gaździcki et al., 1979; Lefeld et al., 1985).
The Lower Liassic (= Grestener Schichten of Uhlig,
1897; Kopieniec Schichten of Goetel, 1917; Kopieniec
Formation of Gaździcki et al., 1979) strata crop out
Fig. 14. Section of the uppermost Fatra and Kopieniec formations in Lejowa Valley. e section shows lithology and distribution of some
important biota components. 1 – dolomites, 2 – limestones, 3 - sandy limestones, 4 – marly limestones, 5 – marls, 6 – shales, 7 – sandstones,
8 – bivalve shells, 9 – crinoids (trochites). A) Exposure of marly shales in the upper part of the formation (hammer for scale); B) Bivalve-
crinoid-gastropod-foraminifer biopelmicrite microfacies; C, D) Benthic foraminifers Ophthalmidium leischneri; x 110; E-G) Palynomorphs:
E) Baculatisporites comaumensis, x 500; F) Schismatosporites ovalis, x 300; G) Quadreaqualina anellaeformis, x 300.
88
A6 — Inception, growth and demise of a pelagic carbonate platform
over a large part of the Sub-Tatric (Krížna) Unit along
the northern slopes of the Tatra Mts (Guzik et al.,
1975, Bac-Moszaszwili et al., 1979; Gaździcki, 2014,
figs 4.4.2, 5.1.1).
In the Lejowa Valley, the Kopieniec Formation is
well exposed on the northeastern slopes of Wierch
Spalenisko Mt. The presented section (Fig. 14) was
traced along the ravine (creek) from Wierch Spaleni-
sko Mt. to Huty Lejowe Glade at the altitude 1040–985
m a.s.l. and rests on the transitional beds of the Rhae-
tian Fatra Fm.
e Kopieniec Formation (up to 100 m thick) is
subdivided into the following informal litostratigraphi-
cal units of the member rank: basal clastics, lower lime-
stones, main claystones, and upper limestones (Fig.
14, see also Gaździcki et al., 1979). Quartz sandstones,
slightly calcareous with clayey-limonitic matrix and
represented in form of distinct layers in the basal part
of the formation are the main lithological type here and
belong to the “basal clastics” of the formation (Gaździcki,
2014, g. 5.1.6). In the upper part of the unit, an assem-
blage of palynomorphs: Baculatisporites comaumensis,
Schismatosporites ovalis, Quadreaqualina anellae-
formis as well as Concavisporites, Dictyophyllites and
Leptolepidites was found in the brown-gray laminated
marly shales (Gaździcki et al., 2006, g. 1) see also Fig.
14E–G). e next unit — “lower limestones” — contains
of dark-grey sandy organodetrital limestones. ese are
bivalve-crinoid-gastropod-foraminifera biopelmicrites
with Pycnoporidium? encrustacions and envelopes. e
spores Globochaete and Eotrix are common. Among the
foraminifera, Ophthalmidium leischneri (Fig. 14B–D),
Planiinvoluta, Nodosaria, Lenticulina and post-Triassic
involutinids predominate (Gaździcki 2014, gs 5.1.8).
Brown-gray shales (claystones) with marly intercalations
prevail in the “main claystones”. e upper unit of the
Kopieniec Formation — “upper limestones” — comprises
a sequence of brown-gray marls, shales and dark-gray
organodetrital limestones (mostly crinoid-ostracod-
brachiopod biointrapelsparite). e limestone inter-
calations contain numerous benthonic foraminifera:
Ophthalmidium leischneri, O. walfordi, Involutina lias-
sica, I. turgida, I. farinacciae and nodosarids (Gaździcki,
2014, gs 5.1.10–11). e uppermost part of the Kopieniec
Formation section is terminated by brown-gray marly
shales with marly intercalations (Fig. 14A).
e clastic-carbonate shallow-marine Late Triassic/
Early Jurassic successions of the Tatra Mts contain bios-
tratigraphicaly important microfossils, mostly foraminif-
era, ostracodes, and conodonts, as well as palynomorphs
and coprolites (Błaszyk and Gaździcki, 1982; Gaździcki,
1974, 1975, 1977, 1978, 1983, 2014; Fijałkowska and
Uchman, 1993). ey have been used to erect local zona-
tions and they may also be of prime importance for region-
al biostratigraphic correlations and palaeogeographic
reconstruction. e recognized evolutionary lineages
and the rapid rates of evolutionary changes of representa-
tives of the benthonic foraminifera families Involutinidae
and Ammodiscidae and the subfamily Ophthalmidiinae
permit an establishment of relatively high resolution zona-
tion. A sequence of two foraminifera zones: Glomospirella
friedli and Triasina hantkeni Zone (aassemblage zone,
Rhaetian) and Ophthalmidium leischneri and O. walfordi
(assemblage zone, Hettangian–?Sinemurian) is recognized
(Gaździcki, 1983). e foraminifera biostratigraphical
zonation of the late Triassic and Early Jurassic in the Tatra
Mts shows that the boundaries of the litostratigraphical
units, i.e. the Fatra- and Kopieniec formations in the Fatri-
cum Domain are diachronous (Fig. 15, see also Gaździcki
and Iwanow, 1976). It may coincide with the Rhaetian-
Hettangian boundary, as was widely assumed, or pass
through the Rhaetian.
Fig. 15. Diachronism of the Fatra and Kopieniec formations in the
Tatra Mts.
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31st IAS Meeting of Sedimentolog y Kraków 2015
e Kopieniec Formation of the Tatra Mts comprises
shallow-marine clastic (with trace fossils which indicate
the Cruziana ichnofacies see Uchman, 1991) and mixed
clastic-carbonate sediments (of tempestitic origin)
deposited in the photic zone (Gaździcki, 2014). e char-
acter of these deposits reects some general changes and
especially epeiric movements at the turn of the Trias-
sic and Jurassic. e sedimentary sequence and oral
and faunal assemblages of the Kopieniec Formation are
almost identical to those from contemporaneous strata
of the Tethys realm. On the other hand, it is possible to
note some similarity to contemporaneous deposits of the
epicontinental basins in the north-western Europe. is
was already noted by Goetel (1917), who emphasized a
marked resemblance to the sandstones with Cardinia
from the Tatra Mts and the Lower Liassic of Swabia in
sedimentary environment and faunal community.
A6.6 Huty Lejowe Glade, Lejowa Valley
– Late Sinemurian-Early Pliensbachian
spotted limestones and marls
(49°15´55˝ N, 19°50´37˝ E)
Leaders: Alfred Uchman, Renata Jach
Bedded grey bioturbated limestones and marly lime- grey bioturbated limestones and marly lime- bioturbated limestones and marly lime-
stones with marl intercalations are characteristic Early
Jurassic, and locally Middle Jurassic, facies in the Krížna
Unit. is hemipelagic facies is an equivalent of the Allgäu
Formation (Fleckenmergel/Fleckenkalk) from the North-
ern Calcareous Alps (e.g., Gawlick et al., 2009). It is called
the spotted limestones and marls in the Carpathians.
An about 150 m-thick series of partly spotty calcilu-
tites and calcisiltites (calcimudstone and wackestones)
interbedded with darker marls is exposed along the
Lejowy Potok stream near Huty Lejowe Glade (Polana
Huty Lejowe) as well as in the lower part of a gully
running from slopes of Pośrednia Kopka Kościeliska
Mt. to Huty Lejowe Glade. According to Lefeld et al.
(1985), the spotted limestones and marls, distinguished
as the Sołtysia Marl Formation, are Early Sinemurian
– Early Pliensbachian in age. eir Sinemurian age is
based on the ammonites Arnioceras falcaries and Arni-
oceras ceratitoides of the Bucklandi Zone (Early Sine-
murian) and Echioceras raricostatum and Echioceras
raricostatoides of the Late Sinemurian Raricostatum
Zone (e.g., Gaździcki and Wieczorek, 1984; Uchman
and Myczyński, 2006). e same deposits are ascribed
as the Janovky Formation in Slovakia (Gaździcki et al.,
1979).
Fig. 16. A fragment of the section of the Sołtysia Marl Formation.
90
A6 — Inception, growth and demise of a pelagic carbonate platform
Proportions of the thickness of limestone beds to
marl interbeds are variable (Figs 16, 17). For this reason
spotted limestones and marls are subdivided into four
subfacies:
• scarce in trace fossils, dark grey marls, interbedded
with dark limestones, with average ratio of marl/lime-
stone bed thickness 4:1 to 1:1. is subfacies occurs in
the lower part of the section and refers to the Przysłop
Marlstone Member (~ 30 m thick);
• bioturbated limestones, interbedded with dark marls,
with marl/limestone bed thickness ratio 2:1 to 1:20.
ese deposits are ascribed to the Pośrednia Hala
Marlstone Member;
• light grey limestones, subordinately interbeded with
thin marls, with rare bioturbational structures. ey
are distinguished as the Pośrednia Kopka Limestone
Member;
• dark grey limestones regularly interbeded with thin
marls, which become strongly silicied toward the
top. Trace fossils are scarce. is facies refers to the
Parzątczak Limestone Member.
e deposits of the Sołtysia Marl Formation contain
relatively common tests of benthic foraminifers, radi-
olarians, ostracods, sponge spicules, whereas macrofos-
sils such as bivalve shells, ammonites, nautiloids and
belemnite rostra are rare (e.g., Gaździcki et al., 1979).
Trace fossils are observed in cross sections as vari-
able dark spots visible against lighter, totally biotur-
bated background (Fig. 17B). Planolites, Chondrites and
alassinoides are common. Zoophycos, Teichichnus,
Taenidium, Phycosiphon (formerly Anconichnus) and
Palaeophycus occur subordinately. e trace fossils were
described by Wieczorek (1995), who supposed that their
tracemakers were controlled by bathymetry, oxygenation
and trophic changes. Wieczorek (1995) distinguished
between two main phases of bioturbation related to
oxygenation changes. During the rst phase, the totally
bioturbated background was produced in well-oxygen-
ated sediment. e fodinichnia-dominated ichnoassem-
blage containing Chondrites, Planolites and Zoophycos is
typical of the second phase, when oxygenation of the sea
oor dropped.
All the trace fossils display typical cross-cutting rela-
tionships. Planolites and alassinoides are cross cut by
Zoophycos, Chondrites and Trichichnus, and Zoophycos is
cross cut by Chondrites and Trichichnus. is order can
be related to vertical partitioning of burrows in sediment
(tiering) and their gradual shi following sediment accu-
mulation or to sequential colonization in time by chang-
ing burrowing communities.
Gaździcki et al. (1979) suggested a depths from deep-
er neritic to bathyal zones for the discussed deposits,
and Wieczorek (1984) interpreted them as basinal but
shallower sediments deposited at the beginning of basin
deepening. e general vertical trend in trace fossils
suggests changes in nutrient supply and oxygenation of
sediments. Also geochemical data, such as the values of
the V/(V+Ni) ratio, comprised between 0.55 and 0.65,
additionally imply changes in oxygen content from oxic
to strongly dysoxic conditions. It is not excluded that the
changes of calcium carbonate content are related to some
climatic oscillations. e limestone-marl alternations
probably reect periodic delivery of siliciclastic material
from adjacent lands. Such a process seems to be climati-
cally dependent probably due to Milankovitch cyclicity
(see Mattioli, 1997).
Fig. 17. Trace fossils from the Sołtysia Marl Formation, Lejowa Valley. A. Vertical cross section. – alassinoides; Ch – Chondrites; Pl –
Planolites; Ta – Taenidium. B. Horizontal section. – alassinoides; Pl – Planolites; Pa – Palaeophycus; Tr – Trichichnus.
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31st IAS Meeting of Sedimentolog y Kraków 2015
A6.7 Długa Valley, Pośrednie ridge –
Middle–Upper Jurassic radiolarites
(49°15´37˝ N, 19°48´04˝ E)
Leaders: Renata Jach, Alfred Uchman,
Nevenka Djerić1, Špela Goričan2,
Daniela Reháková3
1 Faculty of Mining and Geology, Belgrade University,
Belgrade, Serbia
2 Ivan Rakovec Institute of Palaeontology, ZRC SAZU,
Ljubljana, Slovenia
3 Department of Geology and Palaeontology, Faculty
of Natural Sciences, Comenius University, Bratislava,
Slovakia
e Middle–Upper Jurassic radiolarites crop out in
the rock cli located in the Długa Valley along the south-
ern slope of the Pośrednie ridge (Fig. 2). e radiolar-
ite-bearing succession comprises the following facies:
(1) grey spotted radiolarites, (2) green radiolarites, (3)
variegated radiolarites, and (4) red radiolarites (Figs 18;
19A–C). ey are overlain by red limestones. e radi-
olarian-bearing deposits are ~30 m thick.
e radiolarites, on the basis of δ13C, radiolarians and
calcareous dinoagellata are of the Late Bathonian–early
Late Kimmeridgian age (Fig. 18; Unitary Association
Zones 7–11; Moluccana Zone; Polák et al., 1998; Jach et
al., 2012, 2014). e broad negative excursion recorded
Fig. 18. Długa Valley section. Lithology, radiolarian and calcareous dinoagellate biostratigraphy and results for carbon isotope measure-
ments, CaCO3 content and microfacies analysis (aer Jach et al., 2014; modied).
92
A6 — Inception, growth and demise of a pelagic carbonate platform
in spotted radiolarites is Late Bathonian in age, whereas
the pronounced positive δ13C excursion detected in green
radiolarites is referred to Late Callovian. It is worth
mentioning that this excursion coincides with a distinct
increase in radiolarian abundance and an extreme
carbonate production crisis (Bartolini et al., 1999; Moret-
tini et al., 2002). e variegated and red radiolarites and
the overlying limestones display a pronounced decreas-
ing δ13C trend in the Oxfordian–Early Tithonian (Jach
et al., 2014).
e oldest radiolarites are grey and green, highly sili-
ceous, thin- to medium-bedded, alternated with 0.2–2 cm
thick siliceous shales (Fig. 19A, B). ese chert-shale
couplets are the most characteristic feature of the grey and
green radiolarites. Average CaCO3 contents in grey radi-
olarites and in green radiolarites are 36 wt% and 25 wt% ,
respectively (Fig. 18). e grey and green radiolarites show
transition from Bositra-radiolarian to radiolarian micro-
facies, with calcied and extensively dissolved radiolarian
tests (Fig. 19D). Grey spotted radiolarites are intensively
bioturbated whereas green radiolarites locally show subtle
microscopic lamination. e primary lamination can
be referred to incidental rapid sedimentation marked by
a subtle increase in grain size, or a short episode of anoxia.
e variegated and red radiolarites are calcareous,
distinctly bedded, with bed thicknesses of about 10–15 cm
(Fig. 19C). ey have a higher content of CaCO3, 50 wt%
on average (Fig. 18). e common occurrence of massive
chert nodules of various colours, mainly reddish or grey-
ish, is typical of this facies. e very rare occurrence of
thin shale intercalations is characteristic of the vari-
egated radiolarites. e red radiolarites are calcareous,
red and greyish red, and thin- to medium-bedded, with
beds from 5 to 30 cm. e variegated and red radiolarite
facies show upward transition from radiolarian to the
Bositra and Saccocoma microfacies. ey contain calci-
ed or partially silicied radiolarians, sponge spicules,
crinoids, planktonic foraminifera Globuligerina and
cysts of calcareous dinoagellates.
Almost all radiolarite and the associated deposits are
bioturbated (Jach et al., 2012). ey contain the trace
fossils Chondrites, Planolites, Zoophycos, Teichichnus,
Phycodes, Trichichnus, Phycosiphon and alassinoides
(Uchman and Jach, 2014). ey belong to the Zoophycos
ichnofacies, which characterizes deeper shelf – basin
plain settings with pelagic and hemipelagic sedimen-
tation. Generally, the abundance and diversity of trace
fossils decrease up the succession. In the Upper Batho-
Fig. 19. Radiolarites. A) Bioturbated grey spotted radiolarites, polished slab; B) Green radiolarites. polished slab; C) Variagated radiolarites.
polished slab; D) Green radiolarites, radiolarian wackestone-packstone. in section, plane polarised light.
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31st IAS Meeting of Sedimentolog y Kraków 2015
nian–Lower Callovian, the grey spotted radiolarites
display typical spotty structures, that is relatively dense
and diverse cross sections of trace fossils Chondrites,
Planolites, alassinoides, and Zoophycos are common.
Up the succession, in the green, variegated and red facies,
the spots decrease in density, contrast and diversity, up
to disappearance. e changes are not ideally linear, but
uctuations in these features do not discard the general
trend. ey are not related to grain size or lithology.
e changes of ichnological features in the studied
interval are caused mainly by decrease in food content in
the sediments (Jach et al., 2012; Uchman and Jach, 2014).
With deepening of the basin and decreasing sedimenta-
tion rate associated with generally advancing ooding of
epicontinental areas, less and less food was supplied to
the basin from shallower areas and less and less of it was
buried in sediment. In more eutrophic conditions (lower
part of the interval), organisms penetrated deeply in the
sediment, where distinct trace fossils were produced. A
thicker layer of nutritional sediment gave an ecospace
for a higher diversity of burrowing organisms. In more
oligotrophic conditions (higher part of the succession),
the organic matter was concentrated in the soupy sedi-
ment near the sediment-water interface, where preserva-
tion of distinct trace fossils was limited or impossible.
In the Długa Valley section, the Nassellaria/Spume-
llaria (N/S) ratio among radiolarians uctuates, most
probably in accordance with bioturbation intensity
(Jach et al., 2015). It seems that the greater abundance
of trace fossils coincides with the Nassellaria-dominated
assemblage. It is thus possible that the observed pattern
results from ecological requirements of these two groups
of radiolarians. Spumellaria, which tend to be predomi-
nantly symbiont bearing, develop in more oligotrophic
near-surface waters, whereas Nassellaria are non-symbi-
otic forms, which live in more eutrophic, deeper water
column. Such a correlation may be explained by uc-Such a correlation may be explained by uc-
tuating input of nutrients from the neighboring lands,
caused most probably by climate changes, for instance
by enhanced continental weathering and runo (cf.
Baumgartner, 2013). An increased input of nutrients
during humid climate leads to sea-water eutrophication,
whereas decreased input leads to its oligotrophication.
e Late Bathonian–Kimmeridgian radiolarites are
an evidence of deepening, with sedimentation taking
place between the ACD and CCD or below the CCD.
e middle Oxfordian–upper Kimmeridgian, variegated
and red radiolarian-bearing facies, and nally red nodu-red nodu-
lar and platy micritic limestones, record the recovery of
carbonate sedimentation. It is evidenced by the middle
Callovian – lower Oxfordian intervals characterised by
drastically reduced CaCO3 content, whereas an increase
of carbonate content occurs in the middle Oxfordian–
upper Kimmeridgian part of the section.
A6.8 Kryta Valley – Tithonian – Lower
Valanginian limestones and marlstones:
biostratigraphy, magnetostratigraphy,
carbon isotope stratigraphy and
paleoenvironmental changes
(49°15´41˝ N, 19°48´ 20˝ E)
Leaders: Jacek Grabowski, Andrzej Pszczółkowski
The Uppermost Jurassic (Tithonian) and Lower
Cretaceous limestones and marlstones of the Krížna
Nappe crop out in the Kryta Valley and in neigh-
bouring ridges between the Kryta and Długa valleys.
Lithostratigraphically, this interval is divided into
three units (Fig. 20). Shaly marls and olive grey, thin-Shaly marls and olive grey, thin-
ly-bedded micritic limestones occur in the upper part
of the Jasenina Formation (Upper Tithonian to lower-
most Berriasian). The light grey, calpionellid-bearing
limestones of the Osnica Formation (Berriasian) over-
lie the Jasenina Formation deposits. The limestones
are 25–37 m thick in various sections (Pszczółkowski,
1996) and pass gradually into the overlying strata of the
Kościeliska Marl Formation (Lefeld et al., 1985). This
formation, of Late Berriasian-Aptian age, comprises
marls and limestones about 260 m thick (Lefeld et al.,
1985; Pszczółkowski, 2003a; Kędzierski and Uchman,
1997).
Magneto- and biostratigraphic data were obtained
from the Tithonian and Berriasian strata (Fig. 20;
Grabowski, 2005; Grabowski and Pszczółkowski, 2006a),
which enabled correlation of these sections with GPTS
(Geomagnetic Polarity Time Scale), estimation of sedi-
mentation rates and of palaeolatitudinal position of the
area in the Berriasian (28°N, ± 4.5°). Detailed magnetic
susceptibility (MS) and eld gamma ray spectrometry
(GRS), supported by geochemical analyses were used
for reconstruction of palaeoenvironmental changes
(Grabowski et al., 2013, see Fig. 21).
94
A6 — Inception, growth and demise of a pelagic carbonate platform
Stop A6.8.1
Platy, green to grey, micritic limestones of the Jaseni-
na Formation, dipping to the north, are exposed along
the road (Fig. 22).
e thickness of the section amounts to 6 m. In the
lower part limestones prevail, while the upper part is
dominated by marlstones. Limestones contain numerous
remnants of crinoids (Saccocomidae) and chitinoidellids.
e latter microfossils indicate the Boneti Subzone of the
Chitinoidella Zone. e uppermost part of the section
belongs to the Praetintinopsella Zone (Upper Tithonian).
Bed K-1 is reversely magnetized while the bulk of the
section, between beds K-2 and K-17, belongs to a normal
magnetozone (interpreted as M20n). e sedimentation
rate for the Boneti Subzone is estimated as 5.8–7 m/My
(minimum value, without inuence of compaction). In
the neighbouring Pośrednie III section, the sedimenta-
tion rate calculated for entire magnetozone M20n is
Fig. 20. Litho-, bio- and magnetostratigraphic scheme of the Upper
Tithonian and Berriasian of the Lower Sub-Tatric (Krížna Nappe)
succession in the Western Tatra Mts (not to scale), aer Grabowski
and Pszczółkowski 2006b. B – Brodno magnetosubzone (M19n1r);
K - Kysuca magnetosubzone (M20n1r).
Fig. 21. Summary of magnetic and geochemical palaeoenvironmental trends at the Jurassic/Cretaceous boundary interval in the Pośrednie
III section, Western Tatra Mts (aer Grabowski et al., 2013, slightly modied). e transgressive/regressive (T-R) cycles in the Tethyan
domain, aer Hardenbol et al., (1998); paleoclimatic trends in ODP 534 aer Bornemann et al., 2003 and Tremolada et al., 2006; general
paleohumidity trends aer Abbink et al. (2001) and Schnyder et al. (2006). NCE – Nannofossil calcication event.
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31st IAS Meeting of Sedimentolog y Kraków 2015
even lower (4.83 m/My). e distinct rhythm manifested
by marlstone/limestone couplets might be related to
Milankovich cyclicity (precession cycles of ca. 20 ky). e
interval observed represents a local maximum of clastic
input towards the basin. It is characterized by relatively
high MS, high contents of , K and other lithogenic
elements (Al, Ti, Zr, Rb etc.). High values of the /U
ratio, abundant hematite horizons and rather low values
of EF (enrichments factors) Cd/Al, Ni/Al and Mo/Al are
evidences of well oxidized bottom waters. Decreasing
values of productivity indicators (EF P/Al and Mn/Al)
negatively correlate with terrigenous input (Fig. 21). e
interval might be correlated to middle to a late Tithonian
cooling phase evidenced by changes in calcareous phyto-
plankton (Tremolada et al., 2006).
Stop A6.8.2.
We observe micritic limestones with Calpionellopsis
oblonga (Cadisch) indicating the Oblonga Subzone (sensu
Remane et al., 1986) of the Upper Berriasian (Figs 20, 23).
ey belong to the lowermost part of the Kościeliska
Marl Formation. e gradual passage between the
limestone-dominated Osnica and the marl-dominated
Fig. 22. Kryta section of the Jasenina Formation (Kryta Valley).
Praetin. – Praetintinopsella. Aer Grabowski and Pszczółkowski
(2006a). Taxon frequency: 1 – rare; 2 – common.
Fig. 23. Generalized stratigraphical section of the Kościeliska Marl
Formation (lowermost part) in the Kryta Valley. Aer Grabowski
and Pszczółkowski, 2006b, slightly modied. Calpionellid zones
aer Allemann et al. (1971) and Remane et al. (1986). Position of
δ13C event aer Pszczółkowski (2003b) and Pszczółkowski et al.
(2010). 1 – pelagic limestones; 2 –micritic and marly limestones;
3 –marlstones; 4 – sandstones (turbidites); 5 – covered intervals.
96
A6 — Inception, growth and demise of a pelagic carbonate platform
Kościeliska formations is covered in the Kryta creek. In
the section localized in the adjacent Pośrednie ridge and
section Rówienka (in the Lejowa Valley), the boundary
between the two formations is situated in the lower part
of the M16n magnetozone (close to the boundary between
the Simplex and Oblonga subzones; see Fig. 20). e sedi-
mentation rate of the Osnica Formation brackets between
10 and 17 m/My, and increases upward to 18–23 m/My
in the lower part of the Kościeliska Marl Formation. In
this section, the boundary between the Calpionellopsis
and Calpionellites zones (i.e., the Berriasian-Valanginian
boundary) falls in the magnetozone M14r. e Osnica
Formation represents interval of carbonate sedimenta-
tion with limited inux of detrital material (Grabowski et
al., 2013). It is characterized by relatively low MS values,
low contents of and K and other lithogenic elements
(Fig. 21). e interval bears evidence of slightly oxygen-
depleted conditions (low /U ratio, elevated values of
EF Cd/Al, Ni/Al and Mo/Al) and enhanced productiv-
ity (higher EF P/Al and Mn/Al). e phenomena seem to
be coeval with the warming period documented in the
DSDP 534A core in the central Atlantic between magne-
tozones M18r and M17n (Tremolada et al., 2006).
e transition between the Osnica and Kościeliska
formations is manifested again by an increase in sedi-
mentation rate, higher terrigenous inux, lower produc-
tivity and higher redox indices. e latter feature is
independently supported by ichnofossil assemblages
(Kędzierski and Uchman, 1997). e onset of terrig-e onset of terrig-
enous fraction delivery in the Late Berriasian might be
regarded as a regional event within the Krížna (Fatric
Domain) succession in the Slovak part of the Central
Western Carpathians (e.g., Grabowski et al., 2010). It can
be followed as well, in similar stratigraphic position, in
many sections of the Western Tethys: Northern Calcare-
ous Alps, Western Balkan and Western Cuba (Grabowski
and Sobień, 2015).
Stop A6.8.3
e Kryta Member of the Kościeliska Marl Formation
is well exposed in the Kryta creek. is is the stratotype
section of the member, containing marls interbedded
with sandstones and marlstones, 15 m thick (Fig. 23).
The sandstones are mainly medium-grained
lithic and arkosic arenites. However, hybridic aren-
ites also occur (Świerczewska and Pszczółkowski,
1997). Magnetic separation revealed that Cr-spinels
are an important component of the sandstones. The
sandstones occur in similar stratigraphic position in
the Oravice area, Slovakia, just 6–7 km west of our
locality. After this locality, the Oravice event has
been distinguished (Reháková, 2000; Pszczółkowski,
2003b). According to Reháková (2000), the Oravice
event took place in the uppermost part of the Calpion-
ellites Zone which was correlated with the ammonite
Pertransiens Zone. Pszczółkowski (2003a) dated the
sandstones as the upper part of the Calpionellites Zone
Fig. 24. δ13C isotope curve within the uppermost Berriasian –
Hauterivian interval of the Kryta section (aer Pszczółkowski et al.,
2010).
97
31st IAS Meeting of Sedimentolog y Kraków 2015
and the lowermost Tintinopsella Zone (higher part of
the Lower Valanginian).
Rocks of the Meliata suture zone situated to the
(present day) east and/or south east of the Zliechov Basin
(Slovakia) were probably the source of the clastic sediment
(comp. Vašiček et al., 1994). e sedimentation rate within
the Calpionellites Zone is estimated at 28–20m/My.
Stop A6.8.4
Within the upper Valanginian marls of the Kościeliska
Marl Formation, a complete record of the δ13C event
was documented (see Fig. 24; Pszczółkowski, 2001;
Pszczółkowski et al., 2010; see also Kuhn et al., 2005). e
δ13C values increase quickly from the values below 1‰ up
to 2.15‰ close to the lower-upper Valanginian bound-‰ close to the lower-upper Valanginian bound- close to the lower-upper Valanginian bound-
ary. e event occurs in the interval of marly sedimen-
tation and is not marked by any black shale deposition.
is is similar to other Tethyan sections where anoxic
sediments do not occur within the anomaly interval
(e.g., Westermann et al., 2010). e integrated palaeoen-
vironmental study of the Kryta section is in progress,
comprising detailed magnetic susceptibility logging and
geochemical investigations.
Acknowledgments
e eld-trip guide is partly based on the guidebook
prepared on the occasion of 7th International Congress
on the Jurassic System, Jurassic of Poland and adjacent
Slovakian Carpathians (Wierzbowski et al., 2006). is
eld trip is supported by the Tatra National Park (TPN,
Zakopane).
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