Untitled

Blanice Graben
The Blanice Graben is a markedly in NNE-SSW direction elongate half-graben basin structure with steep and
sharp faulted eastern boundary, whereas the western boundary shows relatively low gradient (see Figs 1 and 3).
The basin has been preserved as a discontinuous series of occurrences (denudation remnants) of which the most
important are Český Brod to the north and České Budějovice to the south. Some smaller outcrops near Vlašim,
Divišov and Tábor lie between them. If these occurrences formed continuous sedimentary domain, then the
basin is thought to have been at least 12 km wide and 130 km long. The conspicuous eastern faulted zone is cut
in the north by the E-W trending Kounice fault. To the south it is buried under the České Budějovice Cretaceous
Basin, and extends farther to the south as the Kaplice fault and even farther into Austrian Moldanubicum as the
Rodl fault zone.
Lithostratigraphy
Holub (1972, 1982; Holub in Pešek ed.,in print) distinguished four units in the sedimentary filling: Peklov and
Lhotice Members which form the Černý Kostelec Formation, and the Chýnov and Bulánka Members which
constitute the Český Brod Formation (see Fig.2).
Černý Kostelec Formation
Peklov Member
The Peklov Member consists of mostly grey and red-brown conglomerates, breccias, arkoses and sandstones
attaining a total thickness ranging between 100 and 175 m. Minor are siltstones and claystones. One to two coal
seams 0.2-0.5 m thick are confined to the upper part of the unit in České Budějovice and Český Brod regions.
Holub (in Pešek ed., in print) places the Peklov Member in the Stephanian C.
Lhotice Member
Grey and red-brown sandstones, siltstones and mudstones, attaining a total thickness of 50 - 175 m, are most
abundant in the Lhotice Member. Mostly grey fine-grained sandstones, siltstones and claystones with 1-2 coal
seams, some 0.3-1.2 m thick, occur at the base of the unit. Coal seams were observed in the České Budějovice
region, then near Vlašim (Chobot, Nesperská Lhota) and also in Český Brod region. Holub (in Pešek ed., in
print) rates the Lhotice Member in the lower Autunian.
Český Brod Formation
Chýnov Member
Alternation of red-brown sandstones, arkoses and feldspathic sandstones (a few decimetres thick) with
siltstones, mudstones and claystones is a characteristic feature of the Chýnov Member. Rare are intercalations of
platy clayey carbonates, nodular carbonate layers, grey clayey and silty sediments and bituminous carbonates.
Thickness of the whole formation is believed to be most likely 300 - 500 m but may be even considerably
greater because none of the boreholes drilled in the Český Brod region reached the basement. The Chýnov
Member is likely to be of Late Autunian - Asselian age.
Bulánka Member
The Bulánka Member, or the Bulánka Breccia of some authors, was found to occur exclusively in the Český
Brod region. It is built by mostly by matrix-supported breccia with angular and subangular clasts of rocks of the
Kutná Hora crystalline complex (often the Kouřim orthogneisses), Proterozoic or Early Paleozoic rocks. The
matrix consists of unsorted red-brown clayey feldspathic sandstone to subgraywacke. The Bulánka Member
occurs in a narrow strip rimming the eastern margin of the basin along the Kouřim fault and appears to be
isochronous with the Chýnov Member. However, some authors (Holub 1972, Holub in Pešek ed., in print,
Růžička 1961) are of the opinion that the Bulánka Member is younger than the Chýnov Member. Růžička
(1961) described in the southeastern part of the Český Brod Permocarboniferous (north of Krymov) discordance
1
LITHOLOGY
thickness
MEMBER
C h ý n o v
Č e s k ý
2
3
4
5
6
l o w e r
Lhotice
8
9
Peklov
C
1
7
Černý Kostelec
Steph.
A u t u n i a n
B r o d
upper
AGE
Bulánka
FORMATION
between the older sediments (possibly Chýnov Member) and overlying Bulánka Breccia. But local discordances
can also be interpreted as isochronous interfingering of Bulánka and Chýnov Members.
Fig. 2. Stratigraphy of the Blanice Graben according to Holub (2001). 1. micritic limestone, 2. coal seam and/or
black shale, 3. mudstone, 4. siltstone, 5. sandstone, 6. conglomerate, 7. breccia.
2
Tectonics and kinematic model
The system of eastern marginal faults, which was active during the sedimentation, is a dominant structural
element of the Blanice Graben. Maximum subsidence can be observed along this system. In the Český Brod
region it is represented by the Kouřim fault which is morphologically distinctive. Staňková (1962) reported also
an inverse movement on this fault (subsidence of the eastern block) to have occurred in the Late Cretaceous. The
occurrences near Vlašim and Tábor as well as Permocarboniferous sediments in the České Budějovice region
show a marked faulted contact to the east. This fault zone extends farther to the south as the Kaplice fault and
even farther into Austria as the Rodl fault line.
The E-W oriented Kounice fault is another prominent structural element, which forms the northern border of
Permocarboniferous sediments outcropping in the Český Brod region. This fault is morphologically remarkable
forming the so-called Kounice crest. Here, the northern block subsided in post-Permian times. The Kounice fault
is dissected by several N-S trending faults, which are parallel to the Kouřim fault. Relics of Permocarboniferous
deposits of small thicknesses can also be found north of Kounice fault below marine Cretaceous deposits.
System of smaller E-W and ENE-WSW oriented faults can be seen through the whole basin. Some other faults
of NE - SW strike were discovered during geological mapping (near Klučov and in Český Brod) and along
which some horizontal displacement occurred (Martínek in Zelenka 1999). The basin fill has been deformed and
dissected into single segments by these E-W and NE-SW faults in post-Permian times. The beds are inclined to
the E and NE under 20-30°, exceptionally also to the N or SE or even SW. The segments are separated from
each other by faults along which some considerable movements occurred. For instance, the borehole near
Přistoupim (690 m deep) did not reach the basement, although some outcrops of underlying granite can be
observed nearby (Fig.3). The current relief is partly inverse, mostly modelled by post-Permian tectonic
movements.
Fig. 3. Vertical section of the Blanice Graben south of Český Brod (from Havlena 1964). 1. crystalline complex,
2. Proterozoic, 3. granites, 4. Lower Formation (Černý Kostelec Fm.), 5. Upper Formation (Český Brod Fm.), 6.
limestone horizons, 7. Bulánka Braccia, 8. Upper Cretaceous.
Kinematic model
Brandmayr et al. (1995), basing on studies of mylonitic structures in southern part of the Bohemian Massif,
brought evidence about sinistral late Variscan movement along the Rodl shear zone (NNE-SSW) assuming that
it is one among conjugated Riedl's shears towards the dextral Danube shear zone trending NW-SE (see Fig.4).
The Rodl shear zone showed ductile behaviour in greenschist facies. The 40Ar/39Ar dating on authigenic
muscovite gave values ranging between 288 and 281 Ma. Conspicuous asymmetry of the basin filling and
distribution of lithofacies indicate active synsedimentary eastern fault zone, which was responsible for location
of subsidence axis along the eastern basin boundary. Judging from Brandmayr's et al. (1995) data, it can be
assumed that the dominant orientation of movement on the eastern fault zone was a sinistral horizontal shift.
Therefore, the Blanice Furrow during the sedimentation could have been a system of basins of half-graben type
elongated in NNE-SSW direction, which were opening in transtension regime. These depocenters were likely to
have been separated from each other by hinge zones where no considerable subsidence occurred and thus
sediments might have not been preserved (Fig.5). Present day distribution of faults and their geometries along
3
the Blanice Graben reveal, that the series of sinistral transtensional releasing stepovers is more probable
interpretation rather than sinistral release bends.
Fig. 4. Lithotectonic units and shear zones of the Southern Bohemian Massif. (from Brandmayr et al. 1995).
?
Similar sedimentary systems are described from Dead Sea rift (Bozkurt
2001, Al-Mishwat 2001, and Vita-Finzi 2001) or from the East African
rift zone (Scholz et al. 1993). Because of the lack of paleocurrent data it
is difficult to establish whether the basin was axially drained or whether
there existed isolated subbasins. If the eastern fault zone was propagated
from the south, which is likely providing it was a conjugated Riedl's
shear to the Danube shear zone, then the sedimentation could have been
gradually shifted from the south to the north into the lowest lying
"central under-Cretaceous depression" as suggested by Havlena (1964).
Fig. 5.Kinematic model of the Blanice Graben during Stephanian and Lower Permian.
Depocenters could have been opened as a series of sinistral releasing stepovers.
4
Biostratigraphy
Fauna
Faunal biostratigraphy in Bohemian and Moravian limnic basins is based on aquatic vertebrates (Zajíc 1990,
2000).
Fossils of the Peklov Member (freshwater gastropods) from the Doubravčice locality (Staňková-Růžička 1962)
are known among our limnic basins exclusively from the Blanice Basin and therefore they cannot be used for
stratigraphic considerations. Moreover, their identification is to be taken as being preliminary (Horný 1965).
Consequently, in order to prove the anticipated age (Stephanian C) of the unit it is necessary to obtain fossils of
stratigraphically important animal species (vertebrates, conchostracans, insects). Holub (1966) reported closely
unspecified fauna from dark grey to black-grey bituminous clayey limestone (presumably an equivalent of
fossiliferous bed at the Doubravčice locality) observed in drill cores of the boreholes ČB-3 (Mrzky-West), ČB-6
(Tuchoraz) and ČB-8 (Kšely).
Sediments of the fossiliferous Lhotice Member are known from both the České Budějovice and the Vlašim
denudation remnants of the Blanice Furrow (Table 1). Faunal finds in the České Budějovice region are
connected with former mining for anthracite, particularly in the surroundings of Lhotice. Šetlík (1952) reported
finds of abundant "tiny crustaceans" in dump material of the Lhotice mines. This information, however, cannot
be considered although it is likely that those fossils were ostracodes. The locality "šachta u Lhoty" (shaft near
Lhota), described by Frič (1912), obviously corresponds with the Lhotice mines. Other finds, including the
above-mentioned "tiny crustaceans" have been reported by Šetlík (1952) from the borehole Lhotice-3.
Pelecypods of the Anthracosiidae family from this region are deposited in collections of the National Museum in
Prague. Badly preserved microscopic fossil remains described by Skoček (1993) in carbonate nodules from the
upper section of the Lhotice Member (borehole NVr-1 near Nové Vrátno) go completely beyond so far
mentioned and identified fossils. These finds interpreted as being remains of a marine fauna (radiolaria or
foraminifers, spicules of calcareous sponges, fragments of echinoderms, ostracodes) and plankton flora.
However, Skoček (1993) reports that redeposition of fossils from older or contemporaneous sediments, which
were deposited beyond the boundary of existing occurrences of the Late Paleozoic, cannot be excluded.
Consequently, these finds, due to their problematic origin, are not listed in faunal summary of the Lhotice
Member. Fauna of the Lhotice Member in the Vlašim region has been reported by Daněk (1902), Fritch (1901)
and Havlena (1964) from the localities Chobot near Vlašim and Nesperská Lhota. Since the finds of shark teeth
and scales of actinopterygian fishes are not available, it is difficult to decide about their affinity to a certain
biozone. The material from the Chobot locality is being currently studied. Preliminary results showed large
ostracodes, fragment of insect wing, shark little teeth Triodus cf. carinatus (providing it is really Triodus cf.
carinatus we deal with an equivalent close to the Rudník horizon in the Krkonoše piedmont Basin - the
Asselian), fish scales and bones, coprolites.
Fauna of the Chýnov Member has been described by a number of authors (Daněk 1902, Frič 1912, Holub and
Kozur 1981, Kamarád 1953, Obrhel, Holub and Havlata) from the locality Na Skalce near Český Brod. A part of
this preserved fossil material stored in collections of the National Museum allows to class this fossiliferous
horizon of the Chýnov Member among the earliest Permian Acanthodes gracilis biozone.
Flora
Peklov Member
The oldest known fossil flora of the Blanice Furrow confined to the Peklov Member has been found near
Kostelec nad Černými Lesy. Among typical Stephanian-Permian species the following can, according to Němejc
(1953), be quoted: e.g., Annularia sphenophylloides, A. stellata, Dicksonites plueckenetii, Pecopteris cyathea
and Alethopteris zeilleri. However, no "callipterides" were found there. A few specimens of alethopterides were
described from this locality. They resemble the Alethopteris bohemica species which until recently was not
known from Permian sediments. Pectopteris cyathea is abundant as late as in the Stephanian C but extends into
Permian. On the other hand, no Mixoneura osmundaeformis, which is characteristic of flora of the same age in
the Krkonoše piedmont Basin and Intrasudetic Basin and even in the Boskovice Furrow, was identified in fossil
material at this locality.
Šetlík (1952) identified in material from the Lh-3 borehole near Lhotice, some 170-180 m below the major
anthracite seam, a floral assemblage composed of the same species which accompany the anthracite seam of the
5
Lhotice Member, with the exception of "callipterides" (see further). The spore association, identified by
Kaiserová (1967) in this unit near Tábor, is characteristic of the occurrence of small forms of miospores
(Punctatosporites, Calamospora), apiculate spores of the genera Apiculatisporites and Lophotriletes, monolete
spores of small species (Laevigatosporites) and saccate spores of the genus Florinites or Illinites. The identified
miospores are, according to Valterová, known from both the Westphalian and Stephanian (Table 2).
The occurrence of "callipterides" Autunia conferta and A. naumannii is characteristic of the Lhotice Member
flora in the regions of Český Brod, Vlašim and České Budějovice. However, both species are already known
from the Stephanian of some French basins (Bouroz-Doubinger 1977). Nevertheless, their mass expansion
began as late as in the Autunian. The majority of these species found in the above-mentioned denudation
remnants occur in both the Stephanian and Autunian sediments: Calamites suckowii, Asterophyllites
equisetiformis, Sphenophyllum oblongifolium, Pseudomariopteris ribeyronii, Dicksonites plueckenetii,
Pecopteris cyathea, Callipteridium gigas, Neurocallipteris neuropteroides, Ernestiodendron filicoforme and
Walchia piniformis. Plainly Stephanian elements which do not merge into the Permian are missing in this
assemblage. The occurrence of the Mixoneura osmundaeformis species is interesting because Rieger (1968)
considers this species a Stephanian element. This species was found in an assemblage together with
"callipterides", for instance, in the Intrasudetic Basin and also in the Boskovice Furrow. This species for sure
becomes extinct in the earliest Autunian. Z. Šimůnek considers the assemblage of "callipterides" to be very poor
with advanced species missing.
Chýnov Member
Floral assemblage, described from the locality "Na Skalce" near Český Brod, is, according to Z. Šimůnek, more
or less similar to that occurring in the Lhotice Member. Kaiserová (1967) identified in silty sediments from the
borehole NV-1 miospores of the genera Florinites, Punctatosporites, Cyclogranisporites, Lycospora and
Laevigatosporites.
Palynology of samples from the Bylany locality
Altogether 7 samples were collected at the Bylany locality to be subjected to palynological analysis: sample
no.1 (5.0 m), No.2 (6.15 m), No.3 (7.30 m), No.4 (7.40 m), No.5 (7.55 m), No.6 (7.7 m), No.7 (10.88 - 10. 90
m). The samples were treated using HF, HCL and HNO3 and the obtained macerals showed that samples Nos.37 contain sporomorphs. The list and quantitative proportions of the identified miospores are summarised in
Table 3.
Horizon 7.30-7.70 m (samples Nos.3-6)
Relatively rich assemblage of miospores was separated from a layer of grey silty claystones with plant debris in
which most abundant are bisaccate pollen grains (42%) particularly of the genus Vesicaspora (V.schemeli,
V.ovata) representing coniferous and seed-fern plants (e.g., Autunia conferta species - Kerp 1995). Also
abundant are monosaccate pollen (27%) which belong mostly to coniferous plants and partly to cordaites.The
Potonieisporites genus(P.novicus and P.bhardwaji) is also very abundant. The Florinites genus is present but
except the P.similitis species is rather rare. Striate bisaccate pollen constitutes 7% and the genera Vittatina and
Costaepolllenites 15% of the assemblage. Trilete spores (8%) are represented particularly by the genera
Calamospora (calamites.) , to lesser extent the genera Cyclogranisporites and Convolutispora (pecopterids and
ferns). Sporadic occurrence of the genus Lycospora and Endosporites indicates the presence of lycopod plants.
Horizon 10.88 - 10.90 m (sample No.7)
Miospore spectrum from a tiny layer of the grey silty claystone with plant remains contained 50% bisaccate
nonstriate pollen, 28% Vittatina (genus Costaepolenietes was sporadic). Pollen of seed-fern and coniferous
plants prevailed in palynological spectrum.
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10,88m
10,88m
7,30-70 m
7,30-70 m
0%
10%
20%
30%
40%
50%
60%
70%
Triletes
Monosaccites
Disaccites non striatiti
Disaccites striatiti
Vittatina and Costaepollenites
undeterminable
Sporites
Pollenites
80%
90%
100%
Table 3. Proportion of single groups of miospores in per cent at the Bylany locality (J. Drábková)
Correlation and stratigraphic interpretation/evaluation:
The only information about miospores of Autunian character from the Blanice Furrow is mentioned in a paper
by Konzalová (1970). She found a miospore assemblage in claystones underlying the fresh water Cenomanian
(localities Brník and Kamenná Panna). The assemblage consists mostly of following miospores: Florinites
sp.,Potonieisporites sp., Lueckisporites sp.,Taeniaesporites sp.,aff.,Stroterosporites sp.,Gigantosporites
sp.,Paravesicaspora cf. splendens and Vittatina ovalis .Although the above-quoted miospores are mostly
classified only in genera and their quantitative proportions are not given either, the assemblage appears to be
similar to that identified at the Bylany locality. Other palynological assemblages identified in sediments from the
Blanice Furrow are older (Pešek et al., in print).
The general character and abundant occurrence of the genus Vesicaspora indicate that within the Bohemian
Massif the assemblage of the Kalná horizon appears to be much analogous to the palynological assemblage from
Bylany (Blecha, Martínek et al.1998). The assemblage from the Kalná horizon can be classified as belonging to
Late Autunian palynological zone Disaccites striatiti (Clayton et al.1979). However, higher quantitative
proportion and diversity of striate pollen and the genus Vittatina were found to occur in Bylany, and for the first
time there were identified genera which are common in the Late Permian: genus Luckeisporites (L.cf. L.parvus,
Taeinaesporites, Gigantosporites, et cetera). When compared with the Permian palynological assemblages in
other basins, the Bylany assemblage can be, with certain reservations, classified as belonging to the
palynological zone LO2, established by Doubinger et al. (1987) in the French continental basin de Lodéve
corresponding to the "Saxonian". Kozur (1989) considers this zone as belonging to the upper part of the East
European stage artinsk.
Ichnology
Chýnov Member
Locality: Český Brod - brewery
Distinct and visible ichnofossils were observed in 50% of the local rocks outcropping in the central and
southern part of the locality. The ichnofabric index in these beds attains a value of 2-3. Ichnofossils are mostly
represented by "large Planolites" (alimentary? and access furrows, subhorizontal and inclined without stiffened
walls) and very tiny surface furrows - ichnogenus Unisulcus. Subvertical and vertical components of furrows
with more distinct walls, in one specimen of "U" shape (?ichnogenus Arenicolites) prevail in one bed of more
compact sandstone.
7
Locality: Lstiboř - quarry
Breccia show no visible ichnofabric. Grey siltstones exhibit weak bioturbation - Unisulcus and tiny Planolites,
ichnofabric index = 1-3.
Locality: U Chrášťan - quarry
Coarse-grained breccias show no ichnofabric. Bioturbation was observed only in the uppermost part of strata
sequence in two thin (ca 10 cm) beds of red siltstone. Unisulcus and ? root traces were observed (ichnofabric
index = 2).
Lhotice Member
Locality: Šembera creek
The outcrop shows almost no bioturbation. Only small dark lenses and fragments of siltstone and claystone
developed in form of discontinuous bed contain rare tiny ? root traces and one trace section of Planolites sp. A
?Cochlichnus sp.(surface alimentary or access furrow) was found at the base of red sandstone above one of
some lenses.
Sedimentary record of the Český Brod region
Sediments of the Český Brod denudation remnant of Permocarboniferous are likely to be of the latest
Carboniferous and Early Permian age. They are a part of the Blanice Graben. The outcrops in the central part
(broader vicinity of Český Brod) are built by the Chýnov Member, whereas the Bulánka Breccia rims the eastern
border. The underlying Lhotice Member crops out to the south.
Lithofacies and lateral development
Because of lack of exploration data and insufficient knowledge of the area, the outcropping units are difficult to
be clearly stratigraphically classified. Arkoses in NW part and fine-grained sandstones and siltstones with
intercalations of limestones in the central part are believed to belong to the Chýnov Member of the Český Brod
Formation (Holub 1972). Both units are likely to be just different facies of one stratigraphic unit.
The N-S running basin axis together with E-W trending asymmetry of basin fill control the zonal structure of
lithotypes arranged into N-S trending facies belts. Along the western border of the basin, between Český Brod
and Nová Ves and farther to the south to Tismice, there is possible to distinguish a formation with prevailing
grey arkoses and feldspathic sandstones with intercalations of siltstones and conglomerates. The beds of arkoses
and feldspathic sandstones show often erosional base, occasionally with admixture of pebbles at the bottom.
These sediments exhibit horizontal or trough-cross bedding. These sediments are likely to be products of fluvial
sedimentation. The majority of the area under consideration is covered by red-brown mudstones, clayey
siltstones and clayey fine-grained sandstones which form alternating tens of centimeters thick platy or flat
lenticular beds. These rocks occur in the central part of the Český Brod region, particularly in broader
surrounding of the Český Brod town. Sandstones are massive, having often sharp bases and their upper parts
may exhibit horizontal or ripple bedding. These sediments are mostly products of sand sheets, which were
deposited, in alluvial-lacustrine environment with low gradient. They consist of highly unsorted material, which
indicates relatively fast and stable subsidence during sedimentation. Locally occur cm - 20 cm thick layers of
limestones represented mostly by grey or brown micrite showing traces of lamination. Ostracodes were found in
some beds. Staňková (1961) also reported limestones with sandy admixture and irregular nests of sparite. These
sediments are likely to be carbonates or calcretes originated during soil formation. Grey fossiliferous lacustrine
claystones and clayey and silty sediments with horizons of nodular carbonates occur in the surroundings of
Bylany, whereas grey-black bituminous carbonates accompanied by beds of black claystones were observed
near Tismice.
The Bulánka Breccia builds the eastern boundary of Český Brod "subbasin". It is composed of red-brown,
brown matrix supported breccia. Fragments of cm to 20 cm in size are represented by angular weathered
8
gneisses, granitoids, Lower Paleozoic and Proterozoic shales and quartzites; well-rounded quartz clasts of max.
2 cm in diameter constitute only 1-2% of the rock. The matrix consists of unsorted clayey-silty-sandy material
with relics of strongly weathered rocks. Breccia forms beds some tens of centimeters to a few metres thick, often
massive, occasionally with intercalations of sandstones exhibiting horizontal bedding. The massive, thick,
unsorted beds with high proportion of mud within the breccia matrix are likely to be a product of gravity
currents on an alluvial fan (see Stop 2 - Klučov). While thinner beds with high proportion of sand in matrix and
apparent trough cross bedding are interpreted as products of traction currents at the distal alluvial fan or
proximal braided river (see Stop 3- U Chrášťan).
Petrology
Fragments of limestones found in fields north of Český Brod between the villages of Štolmíř, Černíky and
Kounice are mostly of light brown, grey to grey-black colour shades, micritic massive or with traces of
lamination. More massive samples often contain ostracodes; grey-black fragments show "algal" lamination. Both
observed features indicate sedimentation in lacustrine environment.
In contrast, the samples of nodular carbonates from outcrops in Český Brod (in premises of the former brewery)
and south of Bylany (outer bank of the Bylanka creek) show clear signs of pedogenic sediments. Individual
grains of quartz "float" in microsparite matrix, irregular nests of pedogenic sparite are present, and the material
often contains admixture of Fe-pigment.
Siliciclastic rocks, either coarse-grained feldspathic sandstones or fine-grained silty sandstones collected from
outcrops spread all over the entire area under consideration show similar features. The rocks are poorly sorted,
detritic material consists mostly of subangular quartz, and the content of feldspars varies, whereas muscovite and
Fe-pigment are often abundant. Glauconite was identified in sandstone outcropping in premises of the former
brewery at Český Brod. This mineral is rather rare in continental sediments. Until now only authigenic
glauconite has been described from Holocene lacustrine clays.
Fig.6. Locations of excursion stops. 1. Český Brod – brewery, 2. Klučov, 3. U Chrášťan, 4. Bylany, 5. Šembera
creek.
9
Stop 1 - Český Brod - brewery
Locality is situated in the town of Český Brod in former brewery. Cliff 5 to 10 m high extends towards south for
some 300-400m. Redbrown mudstones, siltstones and fine-grained sandstones of the Chýnov Member of Český
Brod Formation form tens of centimeters thick tabular bodies with
lateral extent many tens of meters along the SE trending cliff. But at
the perpendicular section (trending NE) lensy and flat channel nature
of sandstone bodies can be seen. Paleocurrent data show transport
towards SE. Most mudstones and siltstones are more or less
laminated, with lensy bedding passing to more sandy beds with flaser
bedding. Sandstone bodies are sharp based sometimes with cm - tens
soft
of centimeters erosional relief, typically with trough cross bedding or
sediment
planar cross bedding, rip-up mudstone/claystone clasts can be present
10
deformations
near the base. Upper parts of sandstone beds are ripple or flaser
m
bedded. Laterally persistent mm-cm thick finely laminated claystone
beds are present rarely. Mudstones and siltstones with minor
carb.
sandstone interbeds dominate the section, but thicker sandstone
nodules
succession, composed of several amalgamated sandstone bodies, is
present at the upper part of the section (see fig.7). Section is
moderately bioturbated and several horizons of carbonate nodules of
probably pedogenic origin was found. Sandstones are poorly sorted
with high proportion of clay, muscovite and sericite is abundant,
clayey
detritic biotite can be present as well. Soft sediment deformations
poorly
caused probably by dewatering was also observed in one sandstone
sorted
bed.
Sedimentary structures and vertical succession of lithofacies can be
interpreted as low-gradient alluvial deposits with possible lacustrine
influence. Fluctuation of discharche seems to be apparent. Sandstones
were deposited as sheet-like bodies similar to crevasse splays. Finely
laminated claystones as well as dewatering structures can be evidence
of standing body of water, which can easily produce flaser and lensy
bedding, if we consider low gradient lacustrine mudflat.
Pronounced subvertical fault striking ESE-WSW (022/82) is also
exposed at the cliff. It belongs to the transverse mostly E-W oriented
fault system. Kinematic indicators are unfortunately not preserved,
5
but undulose nature of fault plane may show to the significant strikeslip displacement.
Čes ký B rod - brewery
Stop 2 - Klučov (Bulánka Breccia)
clay
0
Former quarry with Red Army memorial is situated in the vicinity of
the village Klučov by the road to Poříčany. Locality is situated
approximately 2 km from the present day eastern basin margin and
therefore breccias of the Bulánka Member are exposed. Breccia is
matrix supported with poorly sorted clayey sandstone matrix. Clasts
are mostly angular mm to 30cm altered gneisses of (or possible
Proterozoic rocks?), few percent of clasts are composed of
subangular to well rounded quartz. Breccia forms tens of centimeters
to m thick beds, unsorted, with no apparent sedimentary structures
(graded bedding, imbrication). Intercalations of tens of centimeters
thick sandstone beds are present in places. Most of breccia beds was
probably deposited by gravity flows on one of the alluvial fans
fringing eastern basin margin.
c m s fs
Fig. 7. measured section, for explanation see text, for legend see fig.11.
10
K lučov - quarry
NNW
SSE
Fig.8. sketch of the quarry, for explanation see text.
Several faults are exposed, most of them show small vertical displacement as a normal faults. Main fault is
accompanied by several smaller ones all striking NW-SE, two "antithetic" faults in the northern part of the
quarry strike N-S to NNW-SSE (see fig. 8). Unfortunately no kinematic indicators are preserved, but sandstone
according to sandstone marker horizons, vertical displacement along faults is rather small, so strike-slip
component can not be excluded.
Stop 3 - U Chrášťan - quarry
Former quarry is situated by the road Bylany - Chrášťany at the road junction to Lstiboř. Section is dominated
by tens of centimeters thick beds of fine to medium grained breccia and coarse grained sandstones with angular
pebble admixture (see fig.9). fine-grained sandstones and siltstones prevail only in the lowermost part of the
section. Several mm-3cm thick laminated claystone and mudstone beds were also found. Breccia beds are
erosional based, tens of centimeters thick, and typically through cross bedded, only few beds appears massive or
with positive graded bedding. Scale of the outrop (15 m wide, 2-5 m tall) and its 2D nature do not allow precise
distinction of bed geometries, but it seems they form channel and/or scour fills. Breccia clasts are exclusively
angular to subangular, composed of alkali granitoids and aplites (50 %), dark grey quartzite (25%), grey shales
(20%) and subangular quartz (5%). Admixture of clasts much higher than the average of the bed is abundant
(max. 17 cm). Fine grained deposits (siltstones, fine-grained sandstones) are more or less laminated, lamination
is often discontinuous and disturbed. Bioturbation was observed only in the uppermost part of the section in
these fine grained deposits. Lowermost part of the section is characteristic by the presence of dewatering
structures resembling flame and pipe structures. Sandstones can also be ripple bedded. Paleocurrent data are rare
and show transport approximately in N-S direction.
Most of the breccia was deposited by highly energetic traction currents, in some cases gravity flows can be taken
into consideration. Dewatering structures show to rapid deposition and angular nature of clasts to short
transport. Alternations of very different facies can be interpreted as fluctuation of discharge, which may reflect
seasonal, possibly monsoonal climate. Sedimentation took place on the distal alluvial fan or proximal braided
river system. Clast composition is different from the adjoining Kutná Hora crystalline complex and enable
speculation about exotic source rocks not preserved until present.
11
U Chráš ťan - quarry
10
m
5
DEW
DEW
0
cmsfmcfm
sands breccia
Fig. 9. measured section, for explanation see text, for legend see fig.11.
12
Stop 4 - Bylany - Bylanka creek
Outcrop is situated 300 m south of the village Bylany at the bank of the Bylanka creek. Brownish mudstones
and siltstones with several sandstone interbeds dominate lower part of the section (see fig. 10). Mudstones and
siltstones are indistinctly laminated, flaser bedded or bioturbated in places.
Sandstones are cross bedded with rip-up claystone clasts at the base and
flaser bedding or roots near the top. This part of the section represents
probably sedimentation on the alluvial plain or shallow lacustrine
environment.
Upper part of the section is formed mostly by dark grey mudstones with
poorly developed lamination and several cm beds of nodular limestones.
Several sandstone interbeds, and a 1cm thick finely laminated dark grey
claystone bed, are also present. This part of the section is likely to be
deposited in lacustrine environment. Carbonates show features of palustrine
environmment.
Not many fossil species were found at the locality. The bed at the 10.88 m
contained most fossils. One Pteridosperm and a few tens of fragments of
conifers (Walchia) are known from this horizon:
10
Pteridosperma: Mixoneura subcrenulata (Rost), Walchia: Walchia piniformis
m
Schloth, ex Sternb., Ernestiodendron filiciforme (Schloth.), Florin
Culmitzschia speciosa (Florin), Clement-Westerhof (and perhaps also some
other tiny unidentified fragments). A small unidentified seed is known from
the layer ?? 3-5 m. It is very difficult to distinguish the Late Stephanian and
Autunian in their continental development. "Callipterides" were found at the
Stephanian stratotype (Bouroz-Doubinger 1977) but their stratigraphic
importance (at least of some of their species) is somewhat problematic. In
general, the number of Walchia increases with progressing aridization
towards the Permian period to become the dominant group in the Permian.
No "callipterides" were identified at the locality but Walchia were found to
represent a dominant group. More complete assemblage would be necessary
carb.nodules to establish precisely the age. Consequently, it is not clear whether there
occurred only a local sheet erosion and accumulation of plants from higher
lying places or if this xerophilous assemblage reflects regional climate
mudstone
change, and thus is of Permian age. Fauna is represented by carapaces of
carb.nodules
pseudestheriid conchostracans.
B ylanka creek
However, basing on single find of Pteridosperm Mixoneura subcrenulata,
the age of the local sediments would rather correspond to the Late Stephanian
or Early Autunian.
5
Stop 5 - Šembera creek
claystone
Outcrop is situated near the bridge across the Šembera creek by the road from
Kozojedy to Doubravčice. Exposed fine to coarse grained sandstones and
fine grained conglomerates show alternation of highely unsorted beds,
containing large proportion of clays and unstable weathered source rock
material, with moderately to poorly sorted sandstones. Sandstones and
conglomerates are erosional based with pebble admixture, clasts are
subangular to moderately rounded. Flute casts show direction towards ENE.
These beds probably represent fluvial deposition on the lower gradient
western part of the basin. Fluctuation of discharge can also be observed.
0
color
Fig. 10. measured section, for explanation see text, for legend see fig.11.
cmsfm
sands.
13
Š embera creek
3
m
flute casts
0
fmc fm
sands. breccia
L E GE ND:
horiz ontal lamination/bedding
flas er bedding
poorly defined/dis turbed lamination
muddy carbonate
lens y bedding
through cros s bedding
r ipples
plants , plant remains , has h
r oots
r ip-up clas ts (muds tone, clays tone)
admixture of clas ts much larger
than average grain s iz e
DE W
dewatering s tructures
(flame s tr., pipes )
ichnofos s ils
Colors :
grey
brown
dark grey
Fig. 11. measured section, for explanation see text.
14
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15
Appendices
Tab.1. Fauna of the Blanice Graben
Černý Kostelec Fm.
Peklov M.
plži: ?Maturipupa sp., ?Dawsonella sp.
Lhotice M.
mlži: zástupci čeledi Anthracosiidae či Myalinidae
konchostraky: ?Pseudestheria sp.
ostrakodi: Carbonita sp. (původně popsaní jako Bythocypris mytyloides Fritsch, 1901)
žraloci: zuby xenacanthidů
paprskoploutvé ryby: šupiny
Český Brod Fm.
Chýnov M.
konchostraky: Lioestheria paupera (Fritsch, 1901)
mnohonožky: Archiscudderia kopeckyi Frič, 1912
hmyz: křídlo
akantodi: Acanthodes gracilis (BEYRICH, 1848)
paprskoploutvé ryby: šupiny
obojživelníci: ?Branchiosaurus sp., kosti
Tab.2. Flora of the Blanice Graben
Age
Member
Taxon
Steph. C
Lower Autunian
Peklov
?Chýnov
Český Brod region
Kostelec Močidlo,
n. Č. L. Vitice,
Kšely
Český
Brod
Lower Autunian
Lhotice
Vlašim
České Budějovice
region
region
Chobot,
Lhotice, Úsilné
Nesperská vrt Lh 3
Lhota
262-275 m antr. seam
Asolanus camptotaenia Wood
Sigillaria brardii Sternb.
Calamites cruciatus Sternb.
Calamites gigas Brongn.
Calamites multiramis Weiss
Calamites suckowii Brongn.
Annularia pseudostellata Potonié
Annularia sphenophylloides Zenker
Annularia stellata (Schloth.) Wood
Asterophyllites equisetiformis (Schloth.)
Calamostachys germanica (Sternb.)
Sphenophyllum angustifolium (Germ.)
Sphenophyllum longifolium Germ.
Sphenophyllum oblongifolium Germ. et
Kaulf.
Sphenophyllum thonii Mahr
Sphenopteris dechenii Weiss
Pseudomariopteris ribeyronii (Zeill.)
Danzé-Corsin
Dicksonites pluckenetii (Schloth.) Sterzel
Nemejcopteris feminaeformis (Schlotheim)
16
Pecopteris candolleana Brongn.
Pecopteris cyathea (Schloth.)
Pecopteris densifolia (Goepp.)
Pecopteris imbricata Goepp.
Pecopteris lepidorachis Brongn.
Pecopteris plumosa (Artis) Brongn.
Pecopteris polymorpha Brongn.
Pecopteris polypodioides Sternb.
Pecopteris potoniei Němejc
Pecopteris unita Brongn.
Alethopteris bohemica Franke
Alethopteris zeilleri (Ragot) Wagner
Callipteridium gigas Gutbier
Mixoneura osmundaeformis (Schloth.)
Zeill.
Mixoneura subcrenulata (Rost)
Neurodontopteris auriculata (Brongn.)
Potoni‚
Neurocallipteris neuropteroides (Goepp.)
Cleal, Shute et Zodrow
Neuropteris cordata Brongn.
Neuropteris zeilleri Lima
Barthelopteris germarii (Giebel) Cleal et
Zodrow
Autunia conferta (Sternb.) Kerp
Autunia naumannii (Gutbier) Kerp
Taeniopteris abnormis Gutbier
Taeniopteris carnitii Zeiller
Taeniopteris coriacea Goeppert
Cordaites cf. palmaeformis (Goeppert)
Weiss
Cordaites cf. principalis (Germar) Geinitz
Poacordaites sp.
Dicranophyllum sp.
Ernestiodendron filiciforme (Schloth.)
Florin
Walchia piniformis Sternb.
Walchia sp. a (nov. sp.)
Gomphostrobus bifidus (Geinitz.) Zeiller
Samaropsis fluitans Weiss
Samaropsis moravica (Helmh.)
?
Legend:
abundant occurence
documented occurence
?
problematic occurence (cf.)
according Němejc (1953) and Šimůnek (in press)
18
Meters in the sedimentology section on the Bylany locality
7,3-7,7 m
Presence of palynomorfs on the Bylany locality
10,88-90 m
Tab.4.
Calamospora breviradiata KOS.
Calamospora sp.
Cyclogranisporites sp.
Convolutispora sp.
Lycospora sp.
Endosporites formosus KOS.
Nuscoisporites sp.
Florinites minutus BHARD.
Florinites cf. mediapudens (LOOSE) POT et KREMP
Florinites antiquus SCHOPF
Florinites similis KOS.
Florinites sp.
Potonieisporites bhardwaji REMY et REMY
Potonieisporites novicus BHARD.
Potonieisporites sp.
Wilsonites kosankei BHARD.
Vesicaspora ovata (BALME et HENELLY) HART
Vesicaspora schemeli KLAUS
Vesicaspora sp.
Illinites unicus ( KOS.)BHARD.
Scheuringipollenites sp.
Gardenaisporites heiselii KLAUS
Gardenaisporites leonardi KLAUS
Limitisporutes sp.
Platysaccus sp.
Gigantosporites sp.
Kosankeisporites elegans (KOS.) BHARD.
Protohaploxipinus samoilovichii (JANS.) HART
Protohaploxipinus chaloneri CLARKE
Protohaploxipinus sewardi (VIRKKI) HART
Protohaploxipinus sp.
Lueckisporites cf. L. parvus KLAUS
Taeniaesporites sp.
Striatopodocarpites cancellatus (BALME et HENNELLY) CLARKE
Striatopodocarpites sp
Vittatina costabilis WILS.
Vittatina ovalis KLAUS
Vittatina sp.
Costaepollenites elipsoides TSHUDY
Costaepollenites sp.
Presence:
0-2% rare
2-5% infrequent
5-10% frequent
10-25% common
> 25% abundant
18
Tab.5. Palynomorphs from Blanice Graben
Sporonites unionus HORST
Leiotriletes sp.
Calamospora microrugosa (IBR.) S.W. et B.
Calamospora sp.
Punctatisporites sp.
Granulatisporites sp.
Cyclogranisporites jelenicensis KAL.
Cyclogranisporites orbicularis (KOS.) POT. et KREMP
Cyclogranisporites sp.
Planisporites sp.
Lophotriletes sp.
Acanthotriletes sp.
Apiculatisporites sp.(12-33 u)
Apiculatisporites sp.
Verrucosisp. grandiverrucosus (KOS.) SMITH, BUTT. et KNOX
Verrucosisporites sp.
Converrucosisporites sp.
Reistrickia densobaculata KAL.
Reistrickia sp.
Microreticulatisporites sp.
Convolutispora sp.
Lycospora granulata KOS.
Lycospora pusilla KOS.
Lycospora S. W. & B.
Cadiospora magna KOS.
Gravisporites BHARD.
Vestispora costata (BAL.) BHARD.
Cirratriradites saturni (IBR.) S. W. et B.
Laevigatosporites perminutus ALP.
Laevigatosporites minimus (WILS. et COE) S. W. et B.
Laevigatosporites medius KOS.
?
Laevigatosporites desmoinesensis (WILS. et COE) S. W. et B.
Laevigatosporites IBR.
Latosporites globosus (SCHEM.) POT. et KREMP
Latosporites latus (KOS.) POT. et KREMP
19
NV-1 Nová Ves u Chýnova
(Sv. oddíl)
Chý-1 Chýnov
21,9
?
785,50-786,3 NV-1 Nová Ves u Chýnova
VHř 8 Hříva u Louňovic p. Blaníkem
Chobot u Vlašimi
odval - Močedník Bč/4
Dolní Peklov
odval Havírna (Brník) Bč/1
Brník
Chrást u Českého brodu Bč/1
Skalka u Českého Brodu
odval - hájovna Nouzov Bč/3
Nouzov Bč/2
Chýnov
140
Depth (m)
266,00-266,1 ČB - 8 Kšely
Borehole/locality
Český Brod
Vlašim
Český Brod
Černý Kostelec
207,8-207,85 ČB - 6 Tuchoraz
Region
Area
DJ (Drábková); K-K (Kalibová-Kaiserová);
KM (Konzalová); VP (Valterová)
presence:
frequent
rare
NV-1 Nová Ves u Chýnova
(Sv. oddíl)
Chý-1 Chýnov
21,9
K-K1968
K-K1968
K-K1968
VP1989
DJ1998
VP1978
VP1978
VP1978
KM1970
VP1978
DJ1998
?
?
?
common
785,50-786,3 NV-1 Nová Ves u Chýnova
VHř 8 Hříva u Louňovic p. Blan
140
Chobot u Vlašimi
odval - Močedník Bč/4
Dolní Peklov
odval Havírna (Brník) Bč/1
Brník
Chrást u Českého brodu Bč/1
Skalka u Českého Brodu
odval - hájovna Nouzov Bč/3
Nouzov Bč/2
?
VP1978
Author
Chýnov
?
K-K1968
Punctastosporites minutus (IMGR.)POT. et KREMP
Punctastosporites punctatus (KOS.) POT. et KREMP
Punctastosporites pygmaeus (KOS.) POT. et KREMP
Punctastosporites sp.
Speciososporites sp.
Torispora securis BAL.
Torispora undulata DYB. et JACH.
Thymospora thiessenii (KOS) WILS. et VENK.
Thymospora pseudothiessenii (KOS) ALP. et DOUB.
Columnisporites sp.
Spinosporites spinosus ALP.
Endosporites zonalis LOOSE
Endosporites formosus KOS.
Endosporites sp.
Florinites minutus BHARD.
Florinites cf. mediapudens (LOOSE) POT et KREMP
Florinites sp.
Potonieisporites bhardwaji REMY et REMY
Potonieisporites novicus BHARD.
Potonieisporites sp.
Wilsonites kosankei BHARD.
Vesicaspora sp.
Paravesicaspora cf. splendens LESCH.
Illinites unicus ( KOS.)BHARD.
Gigantosporites sp.
Lueckisporites sp.
Taeniaesporites sp.
Stroterosporites sp.
neurčitelné bisakátní
Vittatina ovalis KLAUS
Vittatina sp.
VP1978
Depth (m)
K-K1968
Borehole/locality
266,00-266,1 ČB - 8 Kšely
Český Brod
Vlašim
Český Brod
Černý Kostelec
207,8-207,85 ČB - 6 Tuchoraz
Region
Area
? problematic
raster - index fossils
20
Plate 1. Palynomorphs from the Bylany section
1.
Gardenaisporites heiselii KLAUS
Bylany 7,7 m; 70µm (1000x)
2.
Protohaploxipinus samoilovichii (JANSONIUS) HART
Bylany 10,88-90 m; 67µm (1000x)
3.
Scheuringipollenites sp.
Bylany 7,40 m; 68 µm (1000x)
4.
Taeniaesporites sp.
Bylany 7,7 m; 80µm (1000x)
5.
Striatopodocarpites cancellatus (BALME et HENNELLY) CLARKE
Bylany 7,7 m; 67µm (1000x)
6.
Lueckisporites cf. L. parvus KLAUS
Bylany 7,7 m; 68µm (1000x)
7.
Lycospora sp.
Bylany 7,55 m; 28µm (1000x)
8.
Illinites unicus (KOS.) BHARD.
Bylany 7,55 m; 39µm (1000x)
9.
Kosankeisporites elegans (KOS.) BHARD.
Bylany 10,88-90 m; 47µm (1000x)
10.
11.
Vesicaspora schemeli KLAUS
Bylany 10,88-90 m; 45µm (1000x)
Potonieisporites novicus BHARD.
Bylany 7,30 m; 126µm (500x)
12.
Vittatina costabilis WILS.
Bylany 7,55 m; 41µm (1000x)
13.
? Costaepollenites sp.
Bylany 7,7 m; 31µm (1000x)
14.
Costaepollenites ellipticus TSCHUDY et KOSANKE
Bylany 7,7 m; 45 µm (1000x)
21
Plate 3. Photodocumentation of excursion stops
1. Stop 2 – Klučov quarry; Bulánka Breccia deformed by two systems of normal faults. For
description see text.
2. Stop 3 – U Chrášťan quarry; large breccia clasts floating in sandstone matrix, alkali
granite/aplite and dark grey quartzite and shale clasts can be seen. For description see text.
3. Stop 3 – U Chrášťan quarry; trough cross bedding with large (up to 17 cm) clasts in
breccia bed. For description see text.
4. Lstiboř quarry (close to stop 3); transition from breccia to laminated siltstones and finegrained sandstones.
Plate 3. – cont. Photodocumentation of excursion stops
5. Stop 4 – Bylanka creek; central part of the section showing brownish lower part with tens
of centimeters thick sandstone beds in the lower part and dark grey mudstones with cm
thick nodular limestone beds in the upper part. For description see text.
6. Stop 5 – Šembera creek; flute casts at the base of the unsorted clayey pebbly bed, just
above the hammer. For description see text.
7. Microphotograph of micritic limestone from Bylany; irregular nests of sparite is
characteristic for palustrine carbonates. Magnification 40x, crossed nicols.
8. Microphotograph of micritic limestone from Český Brod; stylolites and ostracod shell.
Magnification 40x, crossed nicols.
9. Microphotograph of arcosic sandstone from Klučov quarry; carbonate cement, and
coroded feldspar (top center) partially replaced by carbonate can be seen. Magnification
50x, crossed nicols.
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