GEOLOGICA CARPATHICA, APRIL 2008, 59, 2, 133—146
www.geologicacarpathica.sk
Introduction
There are several aims of this paper: 1) to summarize for
the first time the existing data on the Lower Badenian red-
algal limestones from the Carpathian Foredeep (CF) in
Moravia (Czech Republic), which so far are dispersed in
various publications and manuscripts; 2) to discuss the
latest own results of field research and macro-/microscopic
studies from 16 outcrops (Prace Hill, Židlochovice,
Podbřežice, Bačov, Sudice, Pamětice, Sebranice, Světlá u
Boskovic, Tišnov-Ochoz, Řepka, Lomnice, Olomouc,
Hostim, Rebešovice, Blučina and Telnice); 3) to evaluate
the obtained data according to contemporary carbonate
sedimentology and actuopaleontology and to use them for
paleogeographical interpretations of the CF in the Early
Badenian.
Geological overview
The Lower Badenian deposits of the Carpathian Fore-
deep (CF) in Moravia (Czech Republic) represent a final
stage of the depositional history of the outer peripheral
basins in the NW of the Central Paratethys. In Middle
and South Moravia, its sediments overlie various blocks
of the Bohemian Massif in front of the flysch nappes. In
North Moravia, Silesia and Poland, they were partially
overthrust by nappes formed during the late Styrian oro-
genic phase. The Lower Badenian is represented by the
basal and marginal psammites and psephites, unstratified
The red-algal facies of the Lower Badenian limestones of the
Carpathian Foredeep in Moravia (Czech Republic)
NELA DOLÁKOVÁ, ROSTISLAV BRZOBOHATÝ, ŠÁRKA HLADILOVÁ and SLAVOMÍR NEHYBA
Institute of Geological Sciences, Faculty of Science, Masaryk University, Kotlářská 2, 611 37 Brno, Czech Republic;
nela@sci.muni.cz; rosta@sci.muni.cz; sarka@sci.muni.cz; slavek@sci.muni.cz
(Manuscript received January 27, 2007; accepted in revised form October 10, 2007)
Abstract: The existing data on Lower Badenian red-algal limestones from the Carpathian Foredeep in Moravia (Czech
Republic), up to now dispersed in various publications and manuscripts, are summarized for the first time. They are
discussed and interpreted according to contemporary carbonate sedimentology and actuopaleontology together with
the latest results of field research and macro-/microscopic studies from 16 outcrops (Prace Hill, Židlochovice, Podbřežice,
Bačov, Sudice, Pamětice, Sebranice, Světlá u Boskovic, Tišnov-Ochoz, Řepka, Lomnice, Olomouc, Hostim, Rebešovice,
Blučina and Telnice). The Moravian red-algal limestones originated in a warm-temperate to subtropical climate and,
in contrast to the Polish part of the Carpathian Foredeep, their areal extent and thickness are distinctly smaller due to
the highly varied basin configuration. The predominating facies of red-algal limestones are biodetrital grainstones
(fine-grained grainstones and bioclastic grainstones), coralline branch rudstones—floatstones and rhodolith rudstones.
Red-algal limestones on the west and northwest margins of the preserved Carpathian Foredeep in Moravia are
connected with the prograding coast line, and their positions in the profiles are not necessarily isochronous. At the
eastern margin of the Carpathian Foredeep (immediately in front of the flysch nappes), important role of the redeposition
of the red-algal limestones into more internal parts of the basin is supposed.
Key words: Middle Miocene, Lower Badenian, Carpathian Foredeep, Czech Republic, paleoecology, paleogeography,
red-algal limestones.
calcareous clays (“Tegel”), red-algal limestones (RAL)
and exceptionally also biohermal bryozoan limestones.
The present-day positions of these sediments represent
only denudation relics of the original sedimentary cover,
more complete ones in the E, markedly reduced ones in
the W, with different postsedimentary tectonic histories
of the various basin parts and even insufficiently de-
tailed correlations of the individual Lower Badenian lev-
els (Fig. 1). Formal lithostratigraphic units have still not
been defined in the Badenian of the CF in Moravia.
RAL (formerly also “Leitha-”, “lithothamnian” or “al-
gal” limestones) are a bio- and lithofacially complicated
complex of rocks forming blocks or lenses in calcareous
clays with Praeorbulina glomerosa and Orbulina sutura-
lis (nannoplankton Zone NN5 – Fig. 1), that represent the
younger part of the Lower Badenian sedimentary cycle
(Rögl et al. 2002). They are geographically situated be-
tween Hostim and Židlochovice in the S and the Moravian
Gateway in the N, or rather between Hostim and Kralice in
the W and the fronts of the flysch nappes in the E. Only
very rare occurrences of Lower Badenian RAL are docu-
mented in the northern part of the Moravian CF (e.g. bore-
hole Kravaře OS-1, Cicha et al. 1985 – Fig. 2).
RAL mainly occur in surficial outcrops, over 50 of
them being known so far from the Moravian part of the
CF (Novák 1975; Jašková 1998, 2002; Zapletal 2004). In
the area between Vyškov and Brno, RAL were also found
in 10 deeper borehole profiles (Fig. 2). The majority of
surficial outcrops are represented only by denudation
relics forming isolated rocks or tapering benches, with
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DOLÁKOVÁ, BRZOBOHATÝ, HLADILOVÁ and NEHYBA
Fig. 1. Stratigraphic position of RAL in Lower Badenian deposits of the Carpathian Foredeep in Moravia (Czech Republic). Calibration
according to Gradstein et al. (2004).
Fig. 2. Positions of the RAL outcrops and boreholes in the Carpathian Foredeep (CF). A – Paleogeography of the Central Paratethys in
the Early Middle Miocene (Goncharova et al. 2004). B – Lower Badenian deposits in the CF. C – Outcrops and boreholes with RAL.
135
RED-ALGAL LIMESTONES OF THE CARPATHIAN FOREDEEP (CZECH REPUBLIC)
thicknesses not exceeding 1 m. Only 2 outcrops quarried
in the past – Světlá u Boskovic and Prace Hill – can be
taken as exceptions. At the locality Světlá u Boskovic
the maximal thickness of RAL in the Moravian part of
the CF ( ~ 44 m) has been verified by boreholes. The RAL
of this locality form boulder-like disintegrating benches,
mutually separated by layers of sands or calcareous clays
and are overlain by calcareous clays (Novák 1975).
Vaněk (fide Novák 1975) distinguished 3 RAL types at
this locality with changing amounts of red algae, repre-
sented predominantly by branched forms with typical
variable sizes of algal clasts, sharply changing even with-
in one and the same layer. At the locality Prace Hill, the
RAL – laterally as well as vertically passing into calcare-
ous sandstones – alternate with parallel laminated sand
beds in a 7 m thick profile (Fig. 4.1,3). The quarried mate-
rial from this locality has also been used for the construc-
tion of the Peace Monument – the memorial to the battle
near Slavkov/Austerlitz in 1805 (Fig. 4.2).
According to their positions within the Lower Bade-
nian depositional succession, RAL are located directly
upon the pre-Badenian basement, either within the cal-
careous clays or overlying them. RAL predominate with-
in the calcareous clays. Only at the outer W and NW mar-
gins, they occur directly upon the pre-Badenian
basement (and often with overlying pelites – Fig. 1).
Overlying the calcareous clays, they can be found practi-
cally only in the outcrops east of Brno (Prace—Holubice—
Kroužek—Židlochovice), often as isolated denudation
relics. According to their relations to the pre-Badenian
basement as well as to the calcareous clays, RAL were
paleogeographically connected with transgression (e.g.
Buday 1955; Hladíková et al. 1992) or regression (e.g.
Cicha & Dornič 1960; Krystek & Tejkal 1968), prospec-
tively with the shallowing of the sedimentary environ-
ment within the shallower neritic area (e.g. Novák 1975)
in a subtropical climate. Only some outcrops of RAL
were analysed in detail from the paleontological point of
view (molluscs, foraminifers, red algae etc.; e.g. Kralice
nad Oslavou – Procházka 1893, Hamršmíd 1984; Prace
Hill, Židlochovice – Zdražílková 1988, Budíková
2003; Bačov, Sudice, Pamětice, Sebranice, Světlá u
Boskovic, Tišnov-Ochoz, Řepka – Zdražílková 1988;
Lomnice – Hudec 1986, Zdražílková 1988; Hostim –
Hladíková et al. 1992; Rebešovice, Blučina, Telnice –
Budíková 2003; Olomouc – Zapletal et al. 2001; Bou-
zov – Panoš et al. 1998; Služín – Vysloužil 1981;
Slatinky – Kupková 1995). Hladil (1976), Hladil in
Cicha (1978) and Hladil in Brzobohatý & Cicha (1978)
processed coral fauna from RAL and calcareous clays.
These data are often accessible in manuscripts only.
In situ biohermal bryozoan limestones were described
only near Podbřežice in the E and Pamětice in the W
(Figs. 2 and 3.1). Their interpretation at Podbřežice
includes depth fluctuations within the shallow water
environment and water temperature changes. At this lo-
cality red algae are almost missing in the lower part of
the bioherm body and gain significance only in its upper
part (Zdražílková 1988; Zágoršek & Holcová 2005).
In the following text the data on the Lower Badenian
RAL from the CF in Moravia are summarized for the first
time significantly specifying the paleogeographical inter-
pretations of the CF in the above mentioned time span.
Methods of study
In the last years our own research was aimed at areally
significant or newly uncovered RAL outcrops (field
research, macro- and microscopic studies – ca. 80 thin
sections): Prace Hill, Židlochovice, Podbřežice, Bačov,
Sudice, Pamětice, Sebranice, Světlá u Boskovic, Tišnov-
Ochoz, Řepka, Lomnice, Olomouc, Hostim, Rebešovice,
Blučina and Telnice. Data obtained in this way are
discussed and interpreted according to contemporary
carbonate sedimentology and actuopaleontology, and
are compared with older paleogeographical studies in the
CF (see also Doláková et al. 2005). The thin sections and
other materials are stored at the Institute of Geological
Sciences, Masaryk University, Brno (abbreviations GU in
Figs. 6—8),
and
at
the
Moravian
Museum,
Brno
(abbreviations MZM in Figs. 6 and 8), Czech Republic.
Results
The studied sediments are represented by RAL with a
changing amount of siliciclastic elements (0—50%)
passing
either
into
calcareous
sandstones
lacking
biogenic component or into completely unsorted facies
with whole rhodoliths and a mixture of micrite, other
organisms and small algal fragments matrix almost
lacking lithoclasts. In some localities (particularly Prace
Hill), clay galls with diameters of even several cm
(Fig. 4.4), often mixed with rhodoliths (Fig. 5.1,2),
frequently occurred.
The dominating fossils are nongeniculate red algae
followed
by
foraminifers
with
calcareous
and
agglutinated
tests.
On
some
outcrops
encrusting
foraminifers of the genus Miniacina were relatively
common among algal crusts in rhodoliths. Large
foraminifers
are
present
in
almost
all
outcrops,
Amphistegina, Heterostegina, and Elphidium, together
with tubes of serpulid worms and bryozoans are
occasionally abundant (Fig. 6), even predominating over
algae at the locality Podbřežice and in some layers of the
locality Prace Hill (Fig. 4.5).
Bivalves, gastropods and echinoderms are abundant
(Figs. 5.2,3, 6.3); ostracods, shark teeth, teeth and scales
of teleosts and brachiopods occur occasionally. Corals
are relatively rare (Fig. 5.1B) – Tarbellastraea and
Heliastraea occur exceptionally (Novák 1975; Hladil
1976) and geniculate red algae are very uncommon (only
the outcrops in the Boskovice Furrow and Olomouc).
Green algae are particularly rare; only a few (2—3) speci-
mens were found.
According to the classification scheme of carbonate
lithofacies (Carranante et al. 1988), the RAL in the Moravi-
136
DOLÁKOVÁ, BRZOBOHATÝ, HLADILOVÁ and NEHYBA
Fig. 3. RAL facies of the studied area. 1 – distribution of individual RAL facies and interpretation of the paleodepths of the Lower
Badenian clays based on otoliths (Brzobohatý 2001); 2 – facies of coralline branch rudstones, Olomouc; 3 – facies of rhodolith
rudstones, Prace Hill; 4 – facies of bioclastic grainstones (visible changes in grain size), Blučina; 5 – rhodolith – the algal bodies
overgrown by bryozoan colonies, Židlochovice; 6 – binding of two adjacent rhodoliths, Prace Hill.
137
RED-ALGAL LIMESTONES OF THE CARPATHIAN FOREDEEP (CZECH REPUBLIC)
Fig. 4. Outcrops of Prace Hill: 1 – the wall of the former quarry – distinct banks of the RAL intercalated by sand layers; 2 – Peace
Monument at the top of Prace Hill built of the RAL material from the former quarry; 3 – sand layer with horizontal lamination –quarry;
4 – the accumulation of clay galls – quarry; 5 – graded beds with bryozoans and red algae – Peace Monument; 6 – graded bed with
rhodoliths – quarry.
138
DOLÁKOVÁ, BRZOBOHATÝ, HLADILOVÁ and NEHYBA
an part of the CF can be interpreted as rhodalgal facies dom-
inated by red algae and bryozoans typical for subtropical to
warm-temperate shelf conditions at the transition between
the tropical zone (chlorozoan and chloralgal lithofacies)
and colder or deeper temperate zone (molechfor lithofacies).
Warm-temperate to subtropical conditions are docu-
mented even in the results of palynological analyses from
the surrounding Badenian calcareous clays. The palyno-
spectra contained representatives of both thermophile (for
example Sapotaceae, Palmae, Engelhardia) and deciduous
Fig. 5. The macroscopic image of RAL samples: 1 – rhodolith rudstones with great clay gall (A) and coral closed in rhodolith (B),
Prace Hill; 2 – the same facies with molluscan fragments, Prace Hill; 3 – the pectinid shells with great rhodolith, Bačov; 4 – rhodolith
rudstones with frequent binding, Prace Hill; 5 – coralline branch rudstones—floatstones, Pamětice; 6 – great symmetrical boxwork
rhodolith, Židlochovice.
arctotertiary floras (Alnus, Ulmaceae, Carya, Juglans). Pa-
lynological studies in the Židlochovice profile confirm
MAT (mean annual temperature) of 15.70—19.40 °C on
the coast of the basin (Bruch et al. 2004).
The predominating RAL facies are as follows:
1. Biodetrital grainstones – detrital facies with litho- as
well as bioclasts that are reworked. These detrital facies
differ mutually in their amount of siliciclastic material and
size of bioclasts. Most of the bioclasts have micritized
rims (Fig. 6.1). Two subtypes were documented:
139
RED-ALGAL LIMESTONES OF THE CARPATHIAN FOREDEEP (CZECH REPUBLIC)
Fig. 6. Fossil organisms in RAL: 1 – bioclastic grainstones with textulariids (foraminifers), Bačov, GU RAL B24; 2 – Amphistegina sp.
and Borelis sp., Světlá, MZM 21A; 3 – echinoid spines, fragment of brachiopod shell, foraminifers, Bačov, GU RAL B5; 4 – overgrowth
of crustose red algae, bryozoans and sessile foraminifers in rhodolith, Prace Hill; 5 – colony of serpulid worms, Židlochovice, GU RAL
Z17; 6 – sessile foraminifers among red-algal thalli, Lomnice, GU RAL L6.
a) fine-grained grainstones – litho- and bioclasts of ap-
proximately the same dimensions, well sorted, without mi-
crite. Algal thalli are preserved only as very small undeter-
minable rounded fragments – unfragmented fossils are
represented only by small foraminifers (Fig. 7.1);
b) packstones to bioclastic grainstones – larger frag-
ments of bioclasts with or without lithoclasts, sometimes
with micrite (Figs. 6.2,3, 7.2).
Occasionally rapid changes of average particle grain-
size within a single layer can be observed (Fig. 3.1,2).
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DOLÁKOVÁ, BRZOBOHATÝ, HLADILOVÁ and NEHYBA
2. Coralline branch rudstones—floatstones with varying
amounts of sparite and micritic groundmass, with bio-
clasts. Some of the samples lack siliciclastic lithoclasts. In
the majority of outcrops fragments of branching forms pre-
vail in thin sections (Figs. 3.2,4, 5.5, 7.3) but very fre-
quently lesser amounts of rhodoliths and fragments of in-
dividual crusts can also be found (Fig. 7.4).
Rhodoliths of this facies comprise a low species diver-
sity, they are exceptionally even monospecific, usually
smaller, but massive, and include few bioclasts. They dis-
play very low primary porosities and lack the matrix
among the crusts, for example, in the outcrops of Lom-
nice (Fig. 7.4) or Olomouc. Only very sporadic encrust-
ing foraminifers and bryozoans can be observed among
the crusts.
According to the character of groundmass and algal
bodies (composed of both fragmented and unfragmented
algal branches and rhodoliths) with various amounts of
siliciclastic grains these facies are considered, after
Rasser (2000), and Rasser & Piller (2004), to have formed
in hydrodynamically protected areas (or in the deeper
areas out of wave current action), whereas the more
detrital facies with sparitic cement probably originated
in areas with higher energy.
In the present-day North Atlantic and the Mediterranean
these sediments are called ‘Maerl’; they are known from
the shallowest subtidal down to the lower limit of the
photic zone (Rasser 2000).
3. Rhodolith rudstones with mostly sparitic cement con-
taining bio- and lithoclasts. The studied rhodoliths have
multispecific growth and the majority of them a “box-
work” internal structure (Basso 1998). The algal crusts of-
ten change with the bryozoan colonies and serpulid tubes
and scarcely with the sessile encrusting foraminifers of
Miniacina (Figs. 3.3,5, 5.6, 6.4,5,6, 7.5,6,7,8). The cavities
between the thalli and borings of several organisms are of-
ten filled with sediment; the binding of two or more small
adjacent algal nodules to the bigger rhodoliths can fre-
quently be observed (Figs. 3.6, 6.2, 7.6). After actuopale-
ontological investigations in the Mediterranean, Southern
Gulf of California and Eastern Australia (e.g. Seneš 1975;
Basso 1998; Halfar et al. 2000; Lund et al. 2000), as well
as after results from the Middle Miocene Polish Korytnica
Basin (Pisera & Studencki 1989), these types of rhodo-
liths develop under conditions of mild water dynamics.
After Basso (1998), the binding of small algal nodules to
the bigger rhodoliths with abundant annelid tubes is typi-
cal for water depths of about 90 m or more.
The locality Prace Hill seems to be a peculiar case –
the rhodoliths are either situated in the sediment
irregularly mixing with clay galls or they form beds in the
rock (Figs. 3.3, 4.6, 5.1,2,4). Sometimes rhodolith-size di-
minishes upwards forming graded bedding – see Fig. 4.6
(Zdražílková 1987). According to Brandano et al. (2005)
or Braga et al. (2006), such a characteristic represents sedi-
ment accumulations transported downslope by gravity
flows and reworked by bottom currents, and occurs, for ex-
ample, on the toe of a carbonate ramp slope. In our case
they can even signal tectonic movements immediately in
front of the flysch nappes (uplift of the Slavkov-Těšín
ridge, Stráník & Brzobohatý 2000).
Among the branching algae as well as among the rhod-
oliths of the coralline branch rudstones—floatstones and
rhodolith rudstones (see facies ad 2), there were some-
times very small unsorted particles of biogenic material,
predominantly also represented by red algae (Fig. 7.7).
According to Flügel (2004), these growth forms manifest
a restricted water energy.
From the systematic point of view, much of the red-
algal thalli are represented only by fragments and they
are undeterminable. In the determinable ones the
Melobesioideae
represented
mainly
by
the
genera
Mesophyllum (Fig. 8.3) and Lithothamnion (Fig. 8.4) are
dominant,
accompanied
by
the
genus Sporolithon
(Fig. 8.5,6) present in low amounts in the majority of
outcrops. Mastoporoideae with the predominance of the
species Spongites albanensis (Fig. 8.2) and Litho-
phylloideae
represented
mainly
by
the
species
Lithophyllum
duplex
(Fig. 8.1)
are
somewhat
less
frequent, but they were found at almost all the localities.
Geniculate red algae were recorded sporadically.
After Braga & Aguirre (2001, 2004), the floristic differ-
entiation of the coralline algae from reef to the temperate
carbonate lithofacies is best marked in shallow-water en-
vironments, where it can be recognized at the subfamily
level. The melobesioids dominate in deep tropical and
shallow to deep temperate environments, usually reaching
depths of 110—120 m. Algal assemblages with Lithotham-
nion and Mesophyllum dominant and Sporolithon com-
mon are characteristic of deep platform environments in
tropical/subtropical conditions. Mastoporoids (for exam-
ple Spongites) dominate in shallow-waters (max. to 40—
50 m) mainly from reef units, being scarce to completely
absent in the assemblages from temperate units. Litho-
phylloids are the most common element of shallow tem-
perate carbonates (Lithophyllum is most abundant in less
than 45 m depths and is scarce to absent below 60 m,
Lund et al. 2000).
On the basis of the above mentioned results, we can
suppose the existence of several different environments
for the origin of RAL in the Moravian part of the
Carpathian Foredeep. The mixture of both lithofacies
and various red-algal subfamilies at the majority of
localities could probably confirm frequent redepositions
from shallower into deeper parts of the basin. Further sys-
tematic studies including the re-descriptions as well as
the precise analyses of the growth forms of the red-algae
at individual localities will be necessary for more de-
tailed interpretations.
Interpretations of depositional environment and
sequence stratigraphy
The transition from the Early to Middle Miocene coin-
cides with significant sea-level fall (Haq et al. 1988;
Hardenbol et al. 1998) and changing tectonic regime in
the Alpine-Carpathian realm (Kováč et al. 2004). Exten-
141
RED-ALGAL LIMESTONES OF THE CARPATHIAN FOREDEEP (CZECH REPUBLIC)
Fig. 7. RAL facies in thin sections. Biodetrital grainstones: 1– fine-grained, highly sorted, without micrite, Řepka, GU RAL R9, 72949;
2 – with greater fragments of bioclasts, Blučina, GU RAL B15. Coralline branch rudstones: 3 – fragments of branched forms,
Olomouc, GU RAL O3; 4 – prevailing branched forms with diffused small compact rhodoliths, Lomnice, GU RAL L2. Rhodolith
rudstones: 5 – multispecific “boxwork” rhodolith with borings of several organisms, Židlochovice, GU RAL Z 18a; 6 – binding of
two adjacent algal and bryozoan nodules to the bigger rhodolith, Prace Hill, GU RAL PV 2b; 7 – several fragmentary rhodoliths with
groundmass lacking lithoclasts, Lomnice, GU RAL L7; 8 – multispecific “boxwork” rhodolith formed by thin crusts and big
interspaces, penetrated by bryozoans and serpulids, Prace Hill, GU RAL PV 1. All scale bars are 2 cm.
142
DOLÁKOVÁ, BRZOBOHATÝ, HLADILOVÁ and NEHYBA
sive marine transgression followed during the early Mid-
dle Miocene (the Early Badenian). All these factors direct-
ly influenced the evolution of basins in the foreland of the
Alpine-Carpathian thrust wedge. Although the ruling fac-
tors of deposition and basin development are widely ac-
Fig. 8. Typical red algae from the studied thin sections. 1 – Lithophyllum duplex Maslov, Lomnice, GU RAL L2,
×100; 2 – Spongites
albanensis (Lemoine) Braga, Bosence et Steneck, Prace Hill, GU RAL PV8,
×200; 3 – Mesophyllum sancti-dionisii Lemoine, Prace
Hill, GU RAL PV1,
×100; 4 – Lithothamnion sp., Pamětice, GU RAL P28, ×100; 5 – Sporolithon sp., Lomnice, GU RAL L10, ×40;
6 – Sporolithon sp., Kroužek, MZM E16A,
×40.
cepted for the broad area of the Central Paratethys (Kováč
2000), opinions about the development of Early to Mid-
dle Miocene sedimentary successions in the two adjacent
foreland basins of the Carpathian Foredeep and the Alpine
Molasse Zone remarkably differ. Numerous authors (Cicha
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RED-ALGAL LIMESTONES OF THE CARPATHIAN FOREDEEP (CZECH REPUBLIC)
1995, 2001; Švábenická & Čtyroká 1998, 1999; Čtyroká
& Švábenická 2000; Švábenická 2002; Rögl et al. 2002;
Ćorić 2003; Ćorić & Rögl 2004; Ćorić & Švábenická
2004; Ćorić et al. 2004) published various statements about
the evolution, biostratigraphy, and chronostratigraphic cor-
relations of the individual sedimentary packages.
The 3
rd
-order depositional sequence was recognized
within the Early Badenian sedimentary infill of the Car-
pathian Foredeep. Tectonic activity combined with eustat-
ic sea-level change were the dominant ruling factors of ba-
sin formation and deposition during the Late Karpatian
and Early Badenian (Nehyba & Šikula 2007). Compres-
sion of the Carpathian orogenic wedge oriented towards
the NNW and NW changed its orientation towards NNE
and NE during the Late Karpatian and Early Badenian
(Kováč 2000). This shift led to the dominant formation of
accommodation space (flexural subsidence) in the north-
ern part of the CF whereas its south-western part (the stud-
ied one) was affected by relative uplift. Older basin infill
(predominantly Karpatian in age) was eroded and de-
formed. A longitudinal depression along the basin axes
(i.e. SW—NE direction – incised valley?) originated, fol-
lowed by formation of coarse-grained Gilbert deltas along
its margins (Nehyba 2006). Gravels, sandy gravels and
gravelly sands (traditionally assigned as “marginal or bas-
al clastics”) are mostly interpreted as deposits of these del-
tas (Nehyba 2001). Such deposits are usually interpreted
as lowstand and/or early-transgressive systems tract in the
sequence stratigraphic models (Zaitlin et al. 1994; Emery
& Myers 1996). Varied presence of tegel intraclasts within
the deposits of coarse-grained Gilbert deltas (Nehyba et al.
2006) and description of deposits of Grund Formation in
some parts of the foredeep (Cicha 1995, 2001; Ćorić &
Rögl 2004) could be the evidence of a more complex po-
sition of these coarse-grained deposits. Stepwise flooding
of the whole Pannonian Basin System during two Early
Badenian transgressions is supposed by Kováč et al.
(2007).
Flooding of the “entire” foreland basin is usually con-
nected with the deposition of a thick pile of basinal
pelites. They are traditionally assigned as “Tegel” and in-
terpreted as shallow marine (shelf) to deep-water (bathyal)
deposits (Brzobohatý 1989). This flooding was connected
with eustatic sea-level change (TB 2.3 – sensu Haq 1991,
CPC 3 – sensu Kováč 2000). Two Early Badenian trans-
gressive phases of sea-level rise are traditionally supposed
in the Carpathian Foredeep (Brzobohatý & Cicha 1993)
with the second one probably more extensive. Lower Bad-
enian basinal pelites can be tentatively interpreted as de-
posits of a transgressive systems tract. RAL are a part of
this transgressive tract. Especially the RAL occurrences
along the western margins of the CF suit this interpreta-
tion (Emery & Myers 1996). Nehyba et al. (in print) pro-
posed subdivision of the “monotonous” pile of Early Bad-
enian basinal pelites into segments with varied positions
within the cycle of relative sea-level change (transgressive
and high-stand systems tract?) and declared an important
role of density currents for their deposition (hyperpyc-
nites?, muddy turbidites).
Both detailed correlations of the Early Badenian sedi-
mentary succession within the Carpathian Foredeep and
their widely accepted lithostratigraphy are still missing.
Inadequate biostratigraphical correlations also complicate
the sequence stratigraphical model of the basin. Facies ar-
chitecture of the varied segments of the basin infill based
on correlations of preserved marginal and basinal facies can
produce reliable sequence stratigraphy and lithostratigra-
phy for the Early Badenian deposits.
In the past, the RAL in the CF were interpreted as
transgressive as well as regressive sediments, indicating
subtropical climate and shallow-water sedimentary con-
ditions (see Geological Overview). These interpretations
were often incompatible with others concerning the sur-
rounding pelites (lower sublittoral and upper bathyal),
according to their foraminifers – Molčíková 1963, and
otoliths – Brzobohatý 2001. The present state of the
Lower Badenian research in the CF enables a somewhat
different interpretation of the RAL.
In general, the studied RAL are situated in two paleo-
geographical positions, namely in the western parts of
the CF, and in the central/eastern parts of the CF.
For the western margins of the CF, isolated relics of
Lower Badenian deposits (Hostim, Kralice, Ptení…) are
more typical than thick accumulations (Světlá). Their or-
igin is connected with the Lower Badenian sea transgres-
sion onto the Bohemian Massif. Relative proximity of
the basin margins can be supposed. Sandy beds occur be-
low the RAL. For this area, the RAL facies of coralline
branch rudstones—floatstones and fine-grained (well sort-
ed) biodetrital grainstones are most typical. They gener-
ally reflect shallow depositional conditions. The RAL of
this part of the CF can be interpreted as both in situ accu-
mulations and erosional blocks redeposited into the ba-
sin. Relatively shallow conditions generally prevailed
and
intrabasinal
paleoheights
(relief)
undoubtedly
played an important role (the individual outcrops seem
to partly form a “rim” along the Drahany Culm – see
Figs. 2 and 3.1).
For the central and eastern parts of the CF, the fairly
continuous preservation of the Lower Badenian deposits
is typical. RAL occur within the mudstone deposits
(“tegels” above and below RAL). In all the studied
borehole
profiles,
the
basal
coarse-grained
Lower
Badenian deposits are absent or occur to a very limited
extent; therefore it seems probable that RAL limestones
are generally connected with places of limited coarse
grained/sand input into the basin. The predominating
RAL facies are biodetrital grainstones and rhodolith
rudstones reflecting relatively deeper conditions. The
absence
of
structures
produced
in
the
coastal
environment within the clastic interbeds is typical. The
sedimentary structures recognized in the associated
clastic deposits (horizontal bedding, normal grading) as
well as some structures within the RAL (presence of
angular clasts, grading, poor sorting) clearly reveal the
important role of sediment gravity currents (debris flows?
– see angular blocks of RAL in the complex position at
Holubice). These currents could be triggered by storms or
144
DOLÁKOVÁ, BRZOBOHATÝ, HLADILOVÁ and NEHYBA
tectonic activity along the active margin of the basin
(Carpathian Flysch). This can explain the RAL positions
within the mudstone beds as well as their variable
positions within the Lower Badenian successions.
Discussion
The above mentioned interpretations even correspond
to the latest conclusions for the Lower Badenian RAL of
the Polish part of the CF where the sedimentation under
temperate
to
subtropical
conditions
is
supposed
(Studencki 1999). Identical features of RAL in Moravia
and in Poland primarily emphasize the systematic
composition of the dominating groups – red algae,
bryozoans, molluscs, worms, echinoids, great foraminifers
– and the total absence of siliciclastic grains. The differ-
ences are represented by distinctly lower thicknesses and
the extent of RAL in Moravia as well as by the total pre-
dominance of “organodetritic limestones” with a low pro-
portion of in situ buildups. This can be caused by the
more differentiated and bathymetrically deeper CF relief
configuration in Moravia. The rather unique presence of
green algae and sporadic but relatively more diversified
hermatypic corals (4 genera, 7 species, only isolated
specimens, no reefs – Hladil 1976) that are almost
completely absent in Poland (Studencki 1999; Górka
2002) indicate the more southern position of the
Moravian part of the CF and the somewhat warmer
conditions. Thus they support the idea of a distinct
climatically controlled N-S gradient in the Lower
Badenian of the Central Paratethys documented in the
decrease both of thermophile molluscs towards N
(Harzhauser et al. 2003) and the gadoid cryophilic fishes
towards S (Brzobohatý et al. 2007). These ascertainments
even correspond to the existence of Lower Badenian coral
reefs which were only documented in more southerly
situated basins (northern Hungary, Styrian Basin, Bulgaria
– Pisera 1996). Nevertheless, the RAL facies of the CF in
Moravia do not exclude some temperature oscillations or
temperature stratification of water. The isotopic studies of
oxygen and carbon (foraminifers, molluscs and carbonate
rocks) done at three outcrops from the Moravian part of
the CF (so far published only from Hostim, Hladíková et
al. 1992) obtained results revealing a wider spectrum of
paleotemperatures, which could be caused not only by
paleoclimatic conditions but also by various positions of
studied localities within the basin. The interpretation of
bryozoans in the profiles at Podbřežice also implies
possible climatic oscillations with a cold period (Zágoršek
& Holcová 2005).
Characters of RAL facies moderate or eliminate even the
discrepancy with the paleobathymetry of the surrounding
calcareous clays based on otoliths (Brzobohatý 2001).
The RAL position inside the calcareous clays is not
necessarily interpretable as a consequence of the bottom
oscillations or the significant sea-level changes. The
interbedding of the algal limestones with the clays could
probably have been caused even by the redepositions of
the rhodoliths and algal bioclasts in deeper parts of the ba-
sin (see above).
Only RAL from the western and north-western margins
of the present occurrences of the Badenian sediments can
be related to the Lower Badenian sea transgression in
Moravia. Nevertheless, their deposition directly upon the
pre-Badenian basement or in its very close proximity as
well as the frequent presence of bathymetrically deeper
overlying clays indicate that they are not connected with
the maximum flooding surface (mfs), but with the pro-
grading coastal line. The picture of RAL distribution on
the present-day western border of the CF is a result of
widespread erosion. This interpretation is confirmed, for
example, by the litho- and biofacial analyses of the lo-
cality Hostim (Hladíková et al. 1992).
Conclusion
Biofacial and lithofacial analyses of the Lower Bade-
nian RAL of the Moravian part of the Carpathian Fore-
deep confirm the sedimentary conditions of warm-temper-
ate to subtropical climate. The sporadic presence of some
groups (corals, green algae) indicates somewhat warmer
waters than in the Polish part of the CF. This fact, together
with the geographical position, documents a transitional
position of the studied area between the northern margin
of the Central Paratethys in Poland and the basins situated
more southerly, and confirms the existence of a N-S orient-
ed climatically dependent gradient with possible short-
term temperature fluctuations in the Central Paratethys.
The areal extents and thicknesses of individual RAL
occurrences in Moravia are distinctly smaller than in Po-
land. They are related to the very different conditions of
basin configuration. The facies with predominating
branched forms of red algae and with sporadic small
compact rhodoliths probably originated in shallower wa-
ters (20—50 m according to the original assumptions).
The facies dominated by rhodoliths with alveolar struc-
tures, bounded, with predominance of serpulids and
Melobesioideae represent somewhat deeper environments.
Sometimes distinct graded bedding in RAL occurrences
on the eastern margin of the CF immediately in front of
the flysch nappes (for example Prace Hill) gives evidence
of downslope transport to greater depths caused by
possible tectonic movements in this area.
The RAL occurrences on the western and north-west-
ern margins of the present shape of the basin can be con-
nected with the prograding coast line, and so their posi-
tions in the profiles need not be isochronous. No
connections of RAL with the regressive tendencies in the
basin have been proved.
Acknowledgments: The authors express their sincere
thanks to J.C. Braga (Granada), M.W. Rasser (Stuttgart),
and an unknown rewiever for critical and constructive
comments on the manuscript. The study was supported by
the Research Project MSM0021622412 (Czech Republic).
145
RED-ALGAL LIMESTONES OF THE CARPATHIAN FOREDEEP (CZECH REPUBLIC)
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