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GEOLOGICA CARPATHICA, 46, S, BRATISLAVA, OCTOBER 1995
285 - 296
EARLY CRETACEOUS SEDIMENTARY CHANGES
IN WEST CARPATfflAN AREA
JOZEF MICHALÍK1, DANIELA ŘEHÁKOVÁ1
and ZDENĚK VAŠÍČEK2
1 Geological Institute, Slovak Academy of Sciences, Dúbravská 9, 842 26 Bratislava, Slovak Republic
2 Department o f Geology and Mineralogy, Mining University, Třída 17. listopadu, 708 33 Ostrava-Poruba, Czech Republic
(Manuscript received March 14, 1995; accepted in revised form June 14, 1995)
Abstrac t: Latest Tithonian bottom relief denivelizalion, local erosion, as well as successive origin of Berriasian/Valangi-
nian carbonate breccias influenced the sedimentary regime of the carbonate basins in Central Western Carpathians. The
Nozdrovice Breccia is interpreted here as the product of sedimentation below an active fault slope. The distribution and
composition of clastic intercalations in hemipelagic carbonate sequences indicate the dynamics of these basins during the
Jurassic/Cretaceous transition.
Key words: Late Jurassic/E arly Cretaceous, Western C arpathians, basin evolution, carbonate sediments, breccias,
microplankton, amm onites.
Z^/ocim
Introduction
Setting
Neocimmerian deformation changed the eustatic and hydrody
namic regime of the Tethyan basins (Michalik 1990). Increased
calcium carbonate production by benthic (reef building) and
planktonie organisms (saccocomas, globochaetes and cal-
pionellids) caused both a gradual increase in the sedimentation
rate and a change of sedimentary lithology (Vašíček et al. 1983,
1994; Michalik & Vašíček 1989; Soták 1989; Michalik et al.
1991; Řeháková & Michalik 1994; Michalik in press).
At the beginning o f the Berriasian, reef growth in the Besky-
dic o f the Western Carpathians ceased. Neritic sediments are
rare (Raptawicka Tumia Formation in the Tatric, pebbles in
younger conglomerates). Prevailing nannocone biomicrites of
the majolica (Pieniny Formation) or biancone types (Oberalm,
Padlá Voda, Osnica and Ladce Formations; Řeháková &
Michalik 1992; Řeháková in press) originated in eupelagic well
aerated conditions. While microplankton skeletons form a sub
stantial constituent of the sediment, remnants of nektonic or
ganisms occur only rarely, benthic fossils are almost missing.
This situation is in accordance with the condition of mass plank
ton development in upwelling sites (Moissette & Saint Martin
1992).
Lithostratigraphy
Studied sections
Results of sedimentological, microbiostratigraphical and corre
lation studies of detailed sampled Jurassic/Cretaceous West-Car-
pathian sections are summarized in Borza & Michalik (1986,
1987), Řeháková & Michalik (1992,1994), Michalik et aL (1994),
Vašíček et aL (1994). The diachronic character of sedimentation
(Boorová 1994), and local erosion (Michalik & Řeháková in
press) make estimation of the J/C boundary difficult.
Seven sections from the Central Western Carpathian Fatric
Zone (Fig. 1) are analysed here: the Strážovce (1; Borza et al.
MASSIF. (Si VIGANTICE
___
VIENNA
BASIN
DAN U ВE
Fig. 1. Localization of sections studied.
286 MICHALÍK, ŘEHÁKOVÁ and VAŠÍČEK
oĺ
cc
CD
marly limestone
thick-bedded limestone
f luxoturbidite layers
cherty limestone
brecciated limestone
Strazov=
Nappe
ZLIECHO
1К г i zna
Nappe
париев т
+ л л г + -+
Fig. 2. Biostratigraphy of the Zliechov section. Fluxoturbidite layers consist of fine detrital limestone with skeletal fragments of shallow - marine
organisms.
4
EARLY CRETACEOUS SEDIMENTARY CHANGES 287
1980), Reváô (2; Řeháková & Michalik 1994) and Zrázy sec
tions (3; Michalik et al. 1993) representing the Zliechov Basin
development (Jasenina, Osnica and Mráznica Formations); the
Zliechov section (4; Fig. 2) with channel development o f the
Osnica Fm; the Nozdrovice (5; Tegernsee, Osnica and
Mráznica Fms; Michalik & Vašíček 1980) and Hlboč sections
(6; Tegernsee, Padlá Voda and Hlboč Fms; Borza & Michalik
1987,1988; Michalik et al. 1988, 1990) in marginal develop
ment of the Zliechov Basin, as well as the Butkov section (7;
Borza et aL 1987; Michalik & Vašíček 1987) in the Manin
elevation (Tegernsee, Ladce, Mráznica Fms).
Uppermost Jurassic formations
a - The Upper Jurassic sequence of the Fatric Zliechov Basin
is represented by the J a sen ina F orm atio n (Michalik et al.
1990). The dark shaly marlstone/marly limestone sequence is
about 30-40 m thick. Irregular allodapic intercalations, more
frequent in the lower part o f the formation, are represented
by thin silt laminae with juvenile aptychi concentrations. The
anomalous sedimentation rates of the uppermost part of the
Jasenina Formation (16.3 mm/Ka in comparison with the
4-7 mm/Ka o f its lower and middle Tithonian part) was prob
ably caused by fine terrigenous imput Planktonie mikroorgan-
isms of the Moluccana, Malmica and Crassicollaria Zones
along with index aptychi indicate a Kimmeridgian/Tithonian
age for the formation.
b -'U p per Jurassic basins were separated by wide flat eleva
tions with nodular Ammonitico Rosso-type limestone sedimen
tation. While the nodular limestones of the Tegernsee F orma
tion represent practically all the Middle and Upper Jurassic
sequence in the Manin Gorge, sedimentation of this type started
as late as in the Callovian in the Butkov (7) and Hlboč (6)
sections (Michalik & Vašíček 1987). Borza & Michalik (1986),
Michalik et al. (1990) and M ichalik & Řeháková (1992) com
pared this formation with the Czorsztyn Formation.
Lowermost Cretaceous formations
a - While the base of ’’Neocomian” well bedded mierite lime
stones of biancone type called the Osnica Formation (Michalik
et aL 1990) is still Late Tithonian in age in the Zrázy, Strážovce,
Osnica and Lúčky sections, this formation was dated as Early
Berriasian (Alpina Subzone: Boorová 1994) in the Motyčky
section near Banská Bystrica. Thus, the character of the bound
ary between the Jasenina and Osnica Fms is diachronic, becom
ing younger southwards into the basin. Similarly, the upper
boundary of the formation also seems to be diachronic: plank-
togene carbonates, the depocentre of which was probably be
low the foot of slope, were gradually thinned by fine terrigenous
admixture basinwards.
b - The Berriasian Padlá Voda Form ation started by erosive
contact with the Tegernsee Formation followed by a sedimen
tary breccia (Borza & Michalik 1987) at the base o f massive
cherty limestones covered by the schistose Hlboč Formation
limestones in the Hlboč section (6; Fig. 3).
с - The Lower Cretaceous hemipelagic sequence starts with
the L adce Form atio n in the Butkov section. Lower clastic
(PI. I: Fig. 1) and upper pelagic members (the latter formed by
thin bedded limestones with brownish limonite spots) are dis
tinguishable in it. Sporadic graded calciturbidite layers occur
in the uppermost part.
Microfacies of lithoclasts
Types of microfacies
Sample sets from each section have been studied by optical
microscope. Two standard microfacies (Wilson 1975) and seven
microfacies types have been recognized in the analysed se
quences: six of them belong to basinal SMF-3 while the re
maining is typical for fluxoturbidites (SMF-4).
MF-a: Saccocoma wackestone to packstone with Saccocoma
sp., Parastomiosphaera malmica Borza, Colomisphaerapulla,
Carpistomiosphaera tithonica, Chitinoidella boneti, Ch. dobeni,
PraetintinnopseUaandrusovi, Globochaete alpina Lomb., crinoid
columnalia, ostracod, aptychi, ammonite, juvenile bivalve frag
ments. It forms breccia clasts in the Butkov and Hlboč sections.
MF-b: Crassicollaria wackestone with Crassicollaria inter
media (Dur. Delga), C. brevis Remane, C. massutiniana (Colom),
С. parvula Remane, Tintinnopsella remanei Borza, T. carpa-
thica (Murg. & Filipescu), Calpionella alpina Lorenz, radio-
larians, Saccocoma sp., globochaetes, juvenile ammonites, ap
tychi, crinoids and bivalve fragments. It forms breccia clasts
in the Hlboč, Zliechov (PL П: Fig. 2), Strážovce, Butkov, Reváň
and Nozdrovice sections.
MF-c: Calpionellid-globochaete (resp. globochaete-cal-
pionellid) wackestone with Calpionella alpina, Rem aniella
ferasini, Nannoconus sp., Crassicollaria parvula, Tintinnop
sella carpathica, Schizosphaerella minutissima (Colom), ra-
diolarians and globochaetes. This type of microfacies forms
Berriasian breccia clasts in all the studied sections (PI. H:
Figs. 1,3-6 ).
MF-d: Nannocomd wackestone w ith Calpionella elliptica
Cadisch, Tintinnopsella carpathica, T. subacuta (Colom),
T. longa (Colom), Remaniela cadischiana (Colom), Calpionel-
lopsis simplex (Colom), C. oblonga (Cadisch), Cadosina fusca
fu s c a Wanner, Colomisphaera vogleri (Borza), C. helios-
phaera (Vogler), radiolarians, ostracods, clay m inerals, py
rite, clastic quartz and glauconite forms breccia c lasts in the
Butkpv- and N ozdrovice section.
MF-e: Nannoconid mudstone with sporadic radiolarians, cal-
pionellids and ostracod fragments. Breccia clasts in the Butkov
and Nozdrovice sections.
MF-f: Radiolarian wackestone to packstone w ith prevail
ing radiolarians and sporadic sponge sp icules, calpionellids
and calcareous dinoflagellates. Breccia clasts in the Butkov
section.
MF-g: Biodetritic grainstone with crinoid, gastropod, bryo-
zoan, bivalve, algae fragments and foraminifers: Nautiloculina
bronnimanni, Pseudocyclammina lithuus, Acruliammina neo-
comiana. Ooids occur sporadically (breccia clasts in the Reváň
section PI. Ш: Figs. 1-6).
Distribution o f the Nozdrovice Breccia M ember
The beginning of the Lower Cretaceous sedimentary cycle
was affected by a Late Cim m erian bottom denivelization
practically in all the sections studied. This influence is trace
able in the proxim al zones (sections 6, 7) marked by non
sedimentation and erosion. Foot breccias originating along
active fault slopes spread laterally through channel fillings
(3) and distal fans (1, 2, 4, 5) far into basins. During the
latest Tithonian to Early Valanginian, a com posite limestone
breccia body described as the Nozdrovice Breccia (Borza et
288 MICHALÍK, ŘEHÁKOVÁ and VAŠÍČEK
Butk o v Hl b o č R e v á ň St rá žov c e
Nozdrovice
В г e c c / a
Z l í e c h o v
■jL" LA 1 ** * 1 v
bioturbated lim esto ne
marly limesto ne
Е Э m i* с г í 11 с limestone
nodular lim estone
detrital limestone
ш brecciated limestone
cherfy lim esto ne
4 j | T 4 lj «« I d
« I t 144 17
Kl (Bem'asian) ^
-------
(Tithonian)
Fig. 3. Litostratigraphical scheme of five Upper Jurassic and Lower Cretaceous sections in the Central Western Carpathians illustrating
distribution of breccia horizons. While the brecciated horizons from shallower areas (Butkov, Hlboč sections) contain wide spectrum of limestone
clasts (MF-a, -b, -c, -d), the composition of breccia layers in deeper basinal areas is more uniform (MF-b, -c).
Jasenina FM
EARLY CRETACEOUS SEDIMENTARY CHANGES 289
al. 1980) with numerous digital apophyses intercalated in the
Osnica, Padlá Voda, Ladce and Mráznica Formations
(Michalik & Řeháková 1994) was formed.
The first carbonate microbreccia layer occurs in the Ber-
riasian Osnica Fm in the Strážovce section (1). Biomicrite
wackestone (MF-b) clasts (1 to 2 mm in size) were mostly
derived from the underlying Jasenina Formation. Breccias
to conglomerates with subangular clasts (0.5 to 10 cm) in the
lower part o f the successive Mráznica Fm come from the Osnica
and Jasenina Fms. The clasts consist of crassicolarian, cal-
pionellid and nannoconid wackestones (MF-b, -c, -d).
Six 18-70 cm thick non-graded limestone breccia layers
crop out in the middle of nannoconid mudstones of the Mráznica
Fm in the Reváň (2) section. Four other marly limestone
layers (100 to 180 cm thick) contain a lot of dispersed he
terogeneous clasts (0.5 -15 cm) of crassicollarian and cal-
pionellid wackestone (MF-b, -c). The occurrence of a 12 cm
sized subangular clast o f biodetrital grainstone (MF-g) is
peculiar. Intercalations (5 0-120 cm) of biodetrital grainstone
of turbidite- and grain-flow origin appear in the higher part
of sequence. Tiny clasts of MF-c, -d microfacies type occur
locally.
Microbreccia packstone intercalation in the Zrázy (No. 3)
section (Michalik et al. 1993) contains Upper Tithonian mi
erite clasts (MF-b), clastic quartz grains and cchinoderm
fragments.
A non-graded brecciated channel filling at the base of the
Zliechov section (4; PI. I: Fig. 2) attains 12 m in thickness.
Its uppermost layers are distorted by synsedimentary slump
ing. The limestone clasts (0.2 to 20-60 cm) were derived
from Upper Tithonian strata (MF-b; PI. П: Fig. 2). The matrix
consists of biomicrite (MF-c) with microplankton association
of the Alpina and Remaniellą Subzones. The considerable
sedimentary rate (72.7 mm/Ka, equal to five to six time the rate
in equivalent sections of neighbourring zones) was caused by
accumulation of limestone breccias filling the channel.
Pelagic nannoconid wackestones prevail in the part of sequence
belonging to the Elliptica, Simplex and Oblonga Subzones. Se
veral turbidite fine detrital limestone intercalations contain lime
stone clasts (MF-d) derived from basemental strata. The decreas
ing sedimentary rate (24.5 mm/Ka) is connected with lower
frequency o f the clastic components. This rate gradually stabi
lized (10.8 mm/Ka) with the surrounding sedimentary basins dur
ing the Calpionellopsis Zone. Turbidite intercalations (MF-g)
amidst pelagic limestones contain limestone clasts (MF-c) coming
from the Lower Berriasian Calpionella Zone strata.
A fine brecciated limestone bed (50-60 cm thick) crops out in
the Lower Valanginian part of the Mráznica Fm in the Nozdrovice
(5) section. The clasts attain size of 1 to 5 mm. Nannoconid
wackestones (MF-d) and mudstones (MF-e) contain clasts of cras
sicollarian wackestones (MF-b), calpionellid-globochaete
wackestones (MF-c) and nannoconid wackestone (MF-d). Borza
in Michalik et al (1979) noted a striking abundance of limestone
clasts belonging to the Elliptica Zone (MF-d). This fact stress the
lithological resemblance of the Nozdrovice sequence with the de
velopment in the Butko v secdoa
The breccia layer covering the Tegernsee Formation in the
Hlboč section (6; Michalik et al. 1990; Michalik & Řeháková
1994) consists of Tithonian limestone clasts (10-20 mm; MF-a,
-b), which eroded (at least) 12 m of underlying beds. The ero
sion is also indicated by calculation o f the sedimentary rates of
the underlying strata: the sediments o f the Lower Tithonian
Malmica, Borzai and Tithonica Zones attain 450 cm in thick
ness, which is equivalent to sedimentary rate of 3.5 mm/Ka.
Similar rates (3 and 3.7 mm/Ka) are also indicated by the thick
nesses o f overlying limestones, belonging to Chitinoidella and
Praetintinnopsella Zones. If it is assumed that the deposition
rate did not substantially change, approximately half of the sedi
mentary column (2.5 m) would be missing. The breccia character
of the Crassicollaria Zone limestones indicates an even higher
deposition rate and even larger deficit of the sediment
Limestone clasts from the base of the massive part o f the
Padlá Voda Fm (10-30, rarely over 70 mm large) were derived
mainly from the Berriasian strata, with smaller share also from
underlying Upper Tithonian beds (Crassicollaria, Calpionella
Zones; MF-b, -c). The breccias in the Lower Valanginian part
of the sequence are exclusively formed by Berriasian limestone
clasts. Their origin indicates an erosion of at least 6- 9 m of the
basemental rock column. Moreover, the calculation of sedimen
tary rate of the Padlá Voda Fm (7 to 11 mm/Ka) indicates a reduc
tion of its lowermost part, belonging to the Афта Subzone by
erosion of ca. 40-50 % (approximately 4- 5 m).
Breccia layers in the higher parts of the Padlá Voda Fm are
predominantly formed by limestone clasts of MF-c, -d, indicat
ing erosion of the Berriasian beds (ca. 5-6 m o f the rock col
umn). The only intercalation in the lowermost part of the over-
lying Hlboč Fm also contains clasts derived from the underlying
limestone strata (MF-d).
The Ladce Formation in the Butkov section (7) starts with a
thick sedimentary breccia containing limestone clasts (1 to 40 mm)
of Tegernsee and Ladce Fms (Michalik & Řeháková 1994). The
contours of clasts often merge with the mierite matrix. The
composition of breccia beds from the gallery No. 11 (153 m)
and No. 12 (170 m) is relatively uniform (MF-c). On the other
hand, somewhat younger breccia from the gallery No. 13 (236m)
contains more variegated clasts (MF-b, -c, -d) coming from a
deeper eroded source. The breccias from the 13th and 14th level
of the Butkov quarry, formed by clasts of MF-a, -b, -d, cover
immediately Lower Tithonian nodular limestones, being followed
by limestones of the Early Valanginian Calpionellites Zone. If
supposed that the breccia was accumulated during the Calpionel
lopsis oblonga Subzone, its thickness (5-6 m) indicates a sedi
mentary rate o f 9.5 mm/Ka The lack o f Upper Tithonian/Bem-
asian sediments (Crassicollaria, Calpionella and Calpionellopsis
Zones) proves an exposed position of this sedimentary area, which
acted as a source of limestone breccias in the adjacent Fatric Basin
until the Late Berriasian.
A similar Early Valanginian gap (lack o f the Calpionellites
Zone) was indicated by Borza (1979) in the marginal Fatric
Belá Unit.
Ammonite taxonomy and biostratigraphy
Breccias at the base of the Ladce Formation (13th level of
the Butkov quarry) contain undeformed, but reworked remains
of cephalopods. This association is dominated by long (Kim-
meridgian to Berriasian, resp. Valanginian) ranging ammonites
like PtychophyUoceras ptychoicum (Quenstedt), Haploceras ex
gr. etimatum (Oppel) and fragments o f evohitely coiled Berriasian
subgenera of Berriasella Uhlig (PL IV: Fig. 7) with simple and
bifurcated ribs. Upper Tithonian Durangites sp. juv. and infre
quent fragments o f the aptychi Lctmellaptychus beyrichi (Op
pel) occur rarely.
Lower part of the Ladce Formation yielded an ammonite
fauna of Haploceras (N.) salinarium Uhlig, PhyUoceras (Ну-
290 MICHALÍK, ŘEHÁKOVÁ and VAŠÍČEK
pophylloceras) ex gr. thetys, Bochianites neocomiensis D’Or-
bigny, Olcostephanus sp. and aptychus Lamellaptychus trauthi
Renz & H abicht. The higher part o f the sequence contains
Haploceras (N.) grasianum (D’Orbigny), Busnardoites cam-
pylotoxus (Uhlig), Kilianelia retrocostata Sayn, K. clavicostata
Nikolov, K. ex gr. pexiptycha (Uhlig) and die aptychi Lamel
laptychus mortilleti (Pictet & Loriol) (Vašíček & Michalik 1986).
The beginning o f a continual pelagic sedimentation interrupted
by sporadic limestone breccia intercalations is dated by am
monites o f the late Early Valanginian Campylotoxus Zone; in
dex ammonites o f the older Pertransiens Zone have not been
found.
Suborder Phylloceratina Arkell 1950
Superfamily Phyllocerataceae Zittel 1884
Family Phylloceratidae Zittel 1884
Genus Ptychophylloceras Spath 1927
Ptychophylloceras ptychoicum (Quenstedt 1849)
PI. IV: Fig. 6.
1849 Ammonites ptychoicus; Quenstedt, p. 219, PI. 17, Figs. 12 a, b
1976 Ptychophylloceras ptychoicum (Quenstedt); Patrulius & Avram,
p. 163, PI. 1, Fig. 8 (cum syn.)
M ate rial: About ten of corroded shell fragments.
Description: Sides of vaulted small involute shells are high,
ventral side is rounded, umbilicus narrow, funnel-shaped.
Corroded remains of a rosette of short constrictions are visible
around umbilicus. They are equivalent to short ventral ribs on
the shell perimeter, stressed by shallow constrictions along their
posterior sides.
Measurements: The specimen illustrated (BK-13/2) with shell
diameter of D - 28.5 mm attains H - 16.0 (0.56), В - 12.9 (0.45).
Distribution : P. ptychoicum ranges from Early Tithonian to
Valanginian. It spread over the whole Mediterranean including
olistolithes of the Tithonian Stramberg Limestone in front of the
Outer Carpathian Magura Nappe in Moravia (Vašíček 1983). In
the central Western Carpathians in red/olive brown breccia on the
base of the Ladce Fm.
Suborder Ammonitina Hyatt 1889
Superfamily Haplocerataceae Zittel 1884
Family Haploceratidae Zittel 1884
Genus Haploceras Zittel 1870
Subgenus Neolissoceras Spath 1923
Haploceras (Neolissoceras) salinanum Uhlig 1888
PI. IV: Figs. 1-2.
1888 Haploceras salinarium n. sp.; Uhlig, p. 104, PI. 5, Figs. 1-3
1902 Haploceras salinarium Uhl.; Uhlig, p. 28,65, PI. 2, Fig. 10
1987 Haploceras (Neolissoceras) salinarium Uhlig; Company, p. 99,
PI. 3, Figs. 1-4; PI. 18, Fig. 3 (cum syn.)
Material: Two molds flattened into a bedding plane. The length
of the body chamber attains something between half (ex. BK-
13/4) or quarter (BK-13/5) of the last whorl.
Description: Small shells with high less vaulted whorls, rela
tively narrow umbilicus and distinct keel along the shell pe
rimeter.
Meas ure m ents: The larger shell attains diameter (D) 22 mm,
the smaller one 21 mm The latter specimen BK-13/5 with maxi
mum whorl diameter is H - 10.0 (H/D - 0.48) and U - 5.2 (U/D
- 0.25). The values measured are influenced by slight lateral
deformation.
Distribution: Company (1987) described abundant Early Vdangi-
nian (late Pertransiens and Campylotoxum Zones) to earliest
Late Valanginian (earliest Vemicosum Zone) occurrences of H.
salinarium from Spain. He introduced the new Salinarium Zone
instead the Campylotoxum Zone. The species is also known
from the Austrian Eastern Alps and Roumanian Carpathians.
In the central Western Carpathians in the Lower Valanginian
part of the Ladce Formation in the Butkov section (Michalik et
al. 1994), in Outer Carpathians in the Kopřivnice Lst in Štram
berk (Houša & Vašíček 1994) and in several Czech and Polish
localities in the Silesian Unit.
Superfamily Perisphinctaceae Steinmann 1890
Family Perisphinctidae Steinmann 1890
Subfamily Paraulacosphinctinae Tavera 1985
Genus Durangites Burckhardt 1912
Durangites sp. juv.
PI. IV: Figs.3-4.
Material: The only fragment o f a corroded sculpture mold
of a juvenile specimen (BK-13/1).
Description: The width of rounded whorls o f evolute shell
is slightly larger than their height. The outer flanks are some
what flattened. The sculpture is mostly form ed by sim ple,
slightly proversional, deflected ribs. However, the juvenile sec
tion of the preserved quarter of whorl is characterised by thick
ventrolateral nodes on each second rib; interribs bear slight
nodes. Ventrolateral nodes in the final section are only indicated
on several ribs. The ribs are not interrupted: an apparent inter
ruption might be caused by corrosion o f the siphonal area. As
well as five simple ribs, one inserted rib reaching the umbilical
area occurs. Complete shell attains diameter around 17 mm. Al
though the morphology of the Butkov specimen resembles
Durangites acanthicus Burckhardt, more precise specification
is hampered by its juvenile growth stage and poor preservation.
Distribution: According to Tavera (1985), the majority of
representatives is typical o f the Late Tithonian Durangites
Zone. The genus survived into the Early Berriasian. It occurs
in basal breccia o f the Ladce Formation.
Aptychi
Lamellaptychus trauthi Renz & Habicht 1985
PI. IV: Fig. 5.
1985 Lamellaptychus trauthi new form; Renz & Habicht, p. 399, PI. 2,
Figs. 12,13
Plate I: Fig. 1. Brecciated limestone bed in the Ladce Formation in
the Butkov section- 13thlevel, magn. 1.7x. Fig. 2. Nozdrovice Brec
cia in the Osnica Formation, Strážovce section, Bed No. 243, magn.
lx. Fig. 3. Brecciated bed in the Mráznica Fm in the Reváň section,
Bed No. 12, magn. 1.3x. Fig. 4. Detto, magn. 1.33x. Fig. 5. Brec
ciated limestone bed in the Osnica Fm in the Zliechov section, Bed
No. 9, magn. 1.44x. Fig. 6. Brecciated limestone with aptychi frag
ments, Vigantice, magn. 1.38x. Fig. 7. Breciated limestone of the
Fasselgraben Fm, Ybbsitz Klippen Belt of the Eastern Alps, Reidl
quarry, 1.6x. Fig. 8. Detto, Csengöhegy near the Zobák Puszta, magn.
l.lx. Fig. 9. Detto, Újbánya Valley,magn. 1.3x.
PLATE I
PLATE II
PLATE III 293
294 MICHALÍK, ŘEHÁKOVÁ and VAŠÍČEK
Plate IV: Figs. 1-2. Haploceras (Neolissoceras) salinarium (Uhlig), 2x. Spec. BK-13a/4 and BK-13a/5, upper part of Lower Valanginian Ladce
Fm, Butkov Quarry, 13th level. Figs. 3 -4. Durangites sp. juv., 3x. Spec. BK-13 br/1. (3-ventral, 4- lateral view). Ladce Fm breccia on Butkov
quarry, 13 th level. F ig. 5. Lamellaptychus trauthi Renz & Habicht, 2x. Spec. BK-13a/8. Upper part of Lower Valanginian Ladce Fm, Butkov
Qu any, 13th level. Fig. 6. Ptychophylloceras ptychoicum (Quenstedt), lx. Spec. BK-13br/2. Reworked mold o f the shell from breccias on 13th
level, Butkov Quan y. Fig. 7. Berriasella sp. indet., 2x. Spec. B K-13br/3. Breccias on 13th level, Butkov Quarry. The specimens were whitened
by the ammonium chloride. The shells figured will be deposited in the collection of Slovak National Museum in Bratislava.
Mate rial: One tiny valve (BK-13/8).
Description: 15 mm long valve with very shallow lateral de
pression All the ribs in the terminal portion bend at a right angle to
the symphysal margin on a relatively wide keel platform However,
just before reaching it, they are arched to the terminal apex.
Distribution: Late Berriasian and Early Valanginian (Swit
zerland; Renz & Habicht 1985). The only valve found in the
Ladce Fm come from its Lower Valanginian part. Incomplete
valves also occur in the Lower Valanginian Tlumačov Marls in
the Kuro vice section.
D is cu s si on
While the Nozdro vice Breccia in the Fatric Zone of the Cen
tral Western Carpathians contains exclusively limestone clasts,
the compositon of isochronous breccias in the neighbouring
areas is more varied.
Píchá & Hanzlíková (1965) described phyllite and gneiss
fragments from calpionellid limestone pebbles in the Ždánice
Unit. Besides limestone clasts, probably ?Penninic Berriasian
limestone breccias known from Belice in Považský Inovec Mts.
(Fig. 1) contain also fragments of crystalline slates (Plašienka
Plate П: Fig. 1. Microbrecciated limestone of the Osnica Fm. Calpionellids, globochaetes and sponge spicules are enclosed in clasts. Zliechov,
43x. Fig. 2. A clast with association of Tithonian microfossils in the Osnica Fm, Zliechov II section, 43x. Fig. 3. Brecciated limestone in the
Osnica Fm. Matrix with microfossils of the Elliptica Subzone contains clasts of Tithonian and Berriasian calpionellid- as well as biogene
limestones. Zliechov -II, 43x. Fig. 4. Brecciated limestone bed in the Mráznica Fm. Reváň section, Bed No. 12, 43x. Fig. 5. A clast with
Calpionella alpina, foraminifers and radiolarians in the Mráznica Fm, Calpionellopsis Zone. Reváň section, Bed No. 12a, 43x. Fig. 6. A clast
with Calpionella alpina and sponge spicules in biomicrite matrix with microfossils of the Calpionellopsis Zone in the Mráznica Fm. Reváň
section, Bed No. 14, 13.5x.
Plate III: Figs. 1-3. Brecciated limestone bed with rich shallow marine detrite in nannoconid mudstone of the Calpionellopsis oblonga Subzone,
Mráznica Fm. Reváň section, Beds Nos. 11 ,12 ,12a,m agn. 13.5x, Fig. 3:43x. Figs. 4-6 . Biodetrite grainstone wiihN autiloculina bronnimanni,
Acruliamm ina neocomiana, bryozoans, bivalve, gastropod and crinoid fragments. A clast in a breccia bed o f the Mráznica Fm. Reváň section!
Bed No. 12b, magn. 13.5x.
EARLY CRETACEOUS SEDIMENTARY CHANGES 295
et al. 1994). Limestone breccias in a small body of Berriasian
limestones near Vigantice (Řeháková et al. 1995) in the Outer
Carpathians also contain (besides of lot of aptychi and crinoid
fragments) clasts of Tithonian and Berriasian limetones, quartz
grains, slate and basic volcanic fragments. Similar brecciated
beds are known also from the Kurovice section (Vašíček &
Řeháková 1994) in the Magura U nit
Berriasian ”Aptychenkalk” (Fasselgraben Formation) from
Reidl quarry in the Ybbsitz Klippen Belt of Eastern Alps con
tains similar limestone breccia w ith Tithonian and Berriasian
limestone clasts, quartz grains and slate fragments. As well as
Upper Jurassic and Berriasian limestone clasts, the brecciated
limestones of the Hungarian MecsekM ts. also contain carbon
ates with Triassic conodonts (S. Kovács, pers. comm.).
The composition o f breccia depended on degree o f tectonic
denivelisation and depth of erosion of the basinal bottom.
Therefore, it can be used as a suitable tool for indication of
synsedimentary tectonic intensity and for the modelling of Neo-
cimmerian environmental dynamics.
Conclusions
The Upper Jurassic and Lower Cretaceous carbonate basins
of the Central Western Carpathians represent a closed deposi-
tionary system consisting of three basic groups of lithofacies
from carbonate platforms through pelagic ramps with plankto-
genous carbonate sedimentation to deep basinal sediments de
posited under anoxic black shale conditions. At the end of the
Tithonian, this system was affected by bottom relief deniveli-
zation, local erosion and by the consequent origin of synsedi
mentary carbonate breccias. Their Late Tithonian to Valangi-
nian age was estimated on the basis of calcareous microplankton
occurring in the matrix. On the other hand, this interval is rep
resented by an erosional gap in several sections. As an example,
the ammonite fauna from the basal breccias of the Ladce For
mation in the Butkov section contains numerous redeposited
Tithonian and Berriasian ammonite fragments. The pelagic up
per part of the Ladce Formation contains Early Valanginian
Busnardoites campylotoxus (Uhlig), higher also Late Valangi
nian indexes Olcostephanus nicklesi Wiedmann & Dieni, Himan-
tocerastrinodosum Thieuloy, Criosarasinella furcillata Thieu-
loy and C. heterocostata (Mandov).
The sedimentary rates of the Berriasian hemipelagic formations
(10-12mm/Ka) depend on the quantity of planktogenous material
deposited Slower sedimentation o f Valanginian and Hauterivian
formations (to 3 mm/Ka) is connected with decreasing diversity
and abundance of microplanktoa Eustatic lowering o f the sea level
caused destruction in the carbonate platform zone as well as trans
port of material by gravitation mechanisms resulting in calcitur-
bidite layers in the basin. On the other hand, the sUiciturbidites
could have originated through river transport penetrating from out
side the depositional system and carrying terrigenous material
from emerged areas. It seems, that the Inna* Carpathian zones on
the south-eastern margin of the Alpine-Carpathian microcontinent
deformed and uplifted by Cimmerian movements were their
source area.
Acknowledgem ents: The paper benefited from critical reading
and valuable comments of Prof. M. M išík and one anonymous
reviewer. Authors thank Mrs. C. Michalíková, H. Brodnianska
and K. Mezihoráková for photographs, and M. Tinková and
E. Kohútová for drawings. The paper contributes to the IGCP
Project 362. It was supported by the Grant Agency of the Slovak
Academy o f Sciences (Grant Project GA 1081).
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