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Excursion guide

- Krkono‰e Piedmont Basin and Boskovice Graben

Faunas and palaeoenvironments of the Late Palaeozoic - Special Publication to 5th Symposium on Permo-Carboniferous FaunasMuseum of Eastern Bohemia at Hradec Králové, July, 7-11, 2008

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Excursion guide - Krkono‰e Piedmont Basin and Boskovice Graben

Stanislav ·tamberg1, Jaroslav Zajíc2, Karel Martínek3, Vladimír Prouza4, Zbynûk ·imÛnek4

1 Museum of Eastern Bohemia at Hradec Králové, Eli‰ãino nábfieÏí 465, 500 01 Hradec Králové, Czech Republic;[email protected]

2 Institute of Geology, Academy of Sciences of the Czech Republic, v.v.i., Rozvojová 269, 165 00 Praha 6 – Lysolaje,Czech Republic; [email protected]

3 Institute of Geology and Paleontology, Charles University, Albertov 6, 128 43 Praha 2, Czech Republic;[email protected]

4 Czech Geological Survey, Klárov 3, 118 21 Praha


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Preface

The aim of the excursion is to introduce participants to palaeogeography, stratigraphy and paleontology of continentalPermo-Carboniferous basins of Bohemian Massif. During excursion the Krkono‰e Piedmont Basin and Boskovice Gra-ben will be visited.The visit of the most instructive localities of the Krkono‰e Piedmont Basin and Boskovice Graben is occasion to discussthe stratigraphy, faunistic content, Late Palaeozoic palaeoenvironment, as well as the relations of the basins of the Bohe-mian Massif to continental basins of Germany or Massif Central in France.The excursion guide represents only the introductory information about stratigraphy and paleontology of visited locali-ties.

We used for preparation of the excursion guide and for the explication on the localities, besides other, the results obtained in the course of following

projects:

DE06P04OMG003 “Actinopterygians from the Permocarboniferous of the Krkono‰e Piedmont Basin” (S. ·tamberg).

RK01P03OMG032 “List of the localities and fauna of the limnic Permocarboniferous basins of Bohemia and Moravia” (S. ·tamberg).

Institutional project Z 3013 0516 (Earth system at the intersection of geological processes, evolution of life, climatic and anthropogenic impacts (J.

Zajíc).

IGCP 491 project (Middle Palaeozoic Vertebrate Biogeography, Palaeogeography and Climate) (J. Zajíc).

GAâR 205/94/0692 “Changes of environment on the Carboniferous and Permian boundary” (J. Zajíc, K. Martínek, J. Drábková, Z. ·imÛnek, M.

Mihaljeviã,J. Hladíková: in BLECHA et al. 1997).

KRKONO·E PIEDMONT BASIN

Krkono‰e Piedmont Basin is located at the north-east of the Bohemian Massif (Fig. 1). The basin was formed as a partof a system of extensional/transtensional basins which opened in the Bohemian Massif during the late phases of theVariscan orogenic cycle. It represents an intramontane depression. The basin is confined by crystalline massifs of theKrkono‰e Mountains on the north, crystalline rocks of Zviãina Hill on the south. The significant Hronov-Pofiíãí Fault onthe east separates the Krkono‰e Piedmont Basin from the Intra-Sudetic Basin. The partial unit of the Krkono‰e PiedmontBasin is the Trutnov-Náchod Subbasin filled with sediments of post-Saalian time.Sedimentary fill of the thickness over 1800m at the central and western parts of the basin, and probably around 2500min the eastern part, is fully non-marine dominated by alluvial and lacustrine strata. The age of this deposits range fromWestphalian D to the Lower Triassic. The lithostratigraphic classification (Fig. 2) is used in the sense of TÁSLER,HAVLENA & PROUZA (1981).The basic layers on the crystalline basement is formed by the sediments of the Kumburk Formation. The upper part ofthe Kumburk Formation is characterized with red and brown coarse-grained arkoses with araucarits (·tikov Arkoses).Overlying Syfienov Formation (Stephanian B) contains several grey layers with thin coal beds. Upper part of Stephanian(Stephanian C) forms Semily Formation. Semily Formation consits of conglomerates on the base and varied siltstones,tuffs, tuffaceous sandstones and bituminous claystones with fauna and flora of PlouÏnice Horizon in the middle part. The


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sedimentation from Semily Formation (Stephanian C) to Vrchlabí Formation (Asselian, Lower Permian) is continuouswithout any hiatus on the large part of the basin, but unconformity is present locally. Vrchlabí Formation contains inaddition to red siltstones and sandstones also very important Rudník Horizon with the rich fauna. Bituminous shales ofthe Rudník Horizon are partly enriched with Cu-sulfides (Bornit, Chalcosine).Freshwater sedimentation continued in Proseãné Formation mainly in reddish siltstones occasionally with tuffaceousadmixture and with intercalated beds of lenticular limestones. Proseãné Formation (Sakmarian) is about 300-400 m thickand represents the finest-grained part of sedimentary basin fill (BLECHA, MARTÍNEK & MIHALJEVIâ 1999). Signi-ficant are layers of bituminous shales and limestones with abundant fauna and flora.Overlying Chotûvice Formation (Artiniskian) represents new cycle of sedimentation and is developped only in the eas-tern part of Krkono‰e Piedmont Basin. The uppermost part of the basin fill represented by Trutnov Formation (Artinis-kian-Kungurian, Saxonian), Bohuslavice Formation (Zechstein, Thuringian) and Bohda‰ín Formation (Triassic) wasdeposited in the Trutnov-Náchod subbasin which formed at the eastern part of the Krkono‰e Piedmont Basin and extendeastwards to the Intra-Sudetic Basin.Volcanic rocks form bedded veins and sheets and constitute the most substantial part of the basin. They consist of basiclavas (melyphyres) as well as intermediate and acid lavas (paleorhyolites).

Stop 1

Locality: PlouÏnice „Railroad cut“ – profile in the railway cut Lomnice nad Popelkou – LibuÀ.Stratigraphy: PlouÏnice Horizon, Semily Formation, Stephanian C.

The section of the total thickness of 60 m crops out at this locality. The dip is 20-25° towards north. On the base of thissection red-brownish calcareous siltstones and sandstones occur, containing bed of dolomitic, partly organodetritallimestone. Overlying horizon, which is traceable for 20 km eastwestwards, consists of grey, variegated, redish and brow-nish, ocasionally mottled siltstones and claystones with cherts and haematitic concretions. The sandstone intercalationsare less in amount. Certain layers exhibit tuffaceous or tuffitic nature.During Stephanian C Krkono‰e Piedmont Basin has probably asymetric structure with steep northern basin margin andlow gradient southern part, which can be documented by the distribution of sedimentary facies of lacustrine PlouÏniceHorizon. Northern part of the basin is dominated by thick anoxic to oxic succesion of lacustrine facies while southernpart of the basin, were the locality PlouÏnice is situated, is characteristic by alternation of suboxic to oxic offshore facieswith nearshore and mudflat facies. Offshore facies representing high lake levels are usually grey to variegated finelylaminated mudstones with volcanogenic admixture in places. Offshore mudstones are often silicified, early diageneticnodular chert beds and lenses can be present. Crystal casts and gypsum pseudomorphs was also found. Nearshore faciesare dominated by sandstone bodies of nearshore bars and sandsheets. Sedimentation during low lake levels was probablydriven by the rate on influx of siliclastic material by ephemeral streams and redistribution of material at the nearshorezone. Southern part of the PlouÏnice lake was surrounded by vegetated mudflats and sandflats while along northern lakemargin swamps were formed locally.

Flora: Plant remains and casts occur in several layers. RIEGER (1968) and ·imÛnek (personal communication) descri-bed: Calamites cistii, Calamites gigas, Calamites suckowii, Annularia stellata, Asolanus camptotaenia, Sigillaria brar-dii, Pecopteris polypodioides, Pecopteris hemitellioides, Pecopteris cyathea, Pecopteris unita, Pecopteris arborescens,Pecopteris cf. lepidorachis, Pecopteris polymorpha, Pecopteris candolleana, Dicksonites plukenetii, Alethopteris bohe-mica, Alethopteris zeilleri, Odontopteris schlotheimii, Odontopteris subcrenulata, Odontopteris brardii, Neurodontopte-ris auriculata, Neurocallipteris neuropteroides, Neuropteris zeilleri, Linopteris germarii, Callipteridium pteridium, Cor-daites borassifolius, Cordaites cf. principalis, Walchia piniformis, Culmitzschia laxifolia, Culmitzschia frondosa var.Zeilleri, Culmitzschia speciosa, Ernestiodendron filiciforme.

Fauna is not well preserved and not abundant. The first description was done by FRITSCH (1879-1901), FRIâ (1912),later by SCHNEIDER (1983), recently by ZAJÍC (2007).Conchostraca: Pseudestheria tenella; Insecta: Neothroblattina germari; Acanthodii: Acanthodes sp.; Elasmobranchii:Sphenacanthus sp.; Actinopterygii: Sphaerolepis kounoviensis, Progyrolepis speciosus, Elonichthys sp., Zaborichthysfragmentalis; Amphibia: branchiosaurs; Tetrapod footprints, coprolites.


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Stop 2

Locality: Kundratice „Doly“Stratigraphy: Rudník Horizon, Vrchlabí Formation, Asselian.

During the Asselian the Krkono‰e Piedmont Basin has assymetric half-graben structure with steep northern marginand gently inclined platform southern margin. Rudník Horizon represents deposits of large stratified anoxic to subo-xic lake which occupy most of the basin area during Lower Asselian. Usually this horizon is composed of about 60m of grey to grey-black mudstones with minor interbeds of carbonates, siltstones, sandstones and conglomerates.Outcrops of the Rudník Horizon in the Krkono‰e Piedmont Basin occur on two flanks. A northern one running fromEast to West along the northern margin of the basin and much shorter southern strip in the area of the village Ko‰Èá-lov occurs.Southern strip is the consequens of tectonic folding. Until recently only the fauna from the southern localities in thearea of Ko‰Èálov (mainly locality Ko‰Èálov „Kováfi’s mill“) has been described (HECKEL 1861, FRITSCH 1879-1901).The outcrop Kundratice „Doly“ represents the section ofthe Rudník Horizon (Fig. 3) where three shallowing-upunits were recognised (MARTÍNEK, BLECHA, DANùKet al. 2005). Unit K1 consists of basal anoxic offshoreblack shales overlain by an offshore, finely laminateddark grey carbonate bed, which passes up into nearlymassive grey mud-cracked nershore carbonate. The topof unit K1 is formed by mudcracked mudstones of themudflat facies. Unit K1 records lake regression accom-panied by carbonate precipitation. Offshore black shalesat the base of the unit K2 sharply overlies the mudflatmudstones of unit K1. The base of black shales is inter-preted as a flooding surface. Black shales representinganoxic offshore sedimentation, are relatively thin andpass gradually into grey laminated mudstones interpretedas having been deposited in more oxygenated offshoresediments. The top of unit K2 is formed by nearshorefacies. Unit K3 shows similar features as the underlyingunits. The basal black shale bed is overlain by a succes-sion of nearshore/mudflat mudstones with interbeds oflenticular, nodular, muddy micritic dolostone beds. Thesedolostone facies are interpreted as beeing precipitatedfrom shallow saline water with the possible influence offresh groundwater. Unit K4 is incomplete, but consists ofrapidly deposited and slumped beds, possibly of volca-nogenic origin, and offshore black shales.

Flora (after ·imÛnek it is the same flora as on the loca-lity Ko‰Èálov „Kováfi’s mill“ – personal communication):Calamites sp., Calamostachys sp., Nemejcopteris femi-naeformis, Pecopteris cf. lepidorachis, Pecopteris poly-morpha, Pecopteris polypodioides, Pecopteris arbores-cens, Pecopteris cyathea, Remia pinnatifida, Odontopte-ris subcrenulata, Autunia conferta, Walchia piniformis,Culmitzschia speciosa.

Fauna: Conchostracans, Acanthodes gracilis, Bohemia-canthus carinatus, Paramblypterus sp., Elonichthys sp.

Fig. 3. Sedimentological section measured at Kundratice„Doly“. For legend see Fig. 4. (After Martínek, Blecha etal. 2005).


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Stop 3

Locality: Vrchlabí „Road cut“ – profile in the road cut W from the town.Stratigraphy: Rudník Horizon, Vrchlabí Formation, Asselian.

The locality at Vrchlabí is one of several interesting outcrops of the northern strip of the Rudník Horizon. At the loca-lity Vrchlabí, which is located at the northern margin of the basin, Rudník Horizon reaches anomalous thickness of130 m, which is due to rapid subsidence rate along steep fault-bounded margin. The determination of thickness is onlyapproximative, because the outcrop is deformed by several small thrust faults. The basement rocks, formed by cry-stalline complex of the Krkono‰e-Jizerské hory Mts., of the Krkono‰e Piedmont Basin, outcrops at the northernmostpart of the Vrchlabí road cut.

Fig.

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Fig. 5. Simplified palaeogeographical sketch of the Krkono‰e Piedmont Basin during the sedimentation of Rudník Lakeshowing distribution of sedimentary environments. Three palaeogeographic elements are recognised: the anoxic offshoreaxial basin, a low-gradient mudstone/carbonate dominated southwest margin, and high-gradient northern margin withgravity driven deposits. Circle refer to the studied localities and boreholes (Fig. 1). (After Martínek, Blecha et al. 2005).

Fig. 6. Depositional model of the Rudník Lake during a lake-level highstand. Facies architecture was controlled mainlyby subsidence along the northern marginal fault. (After Martínek, Blecha et al. 2005).


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Two distinctive units are recognised at the outcrop (MARTÍNEK, BLECHA, DANùK et al. 2005).At the base of the section (Fig. 4 ), mottlled mudstones with carbonate nodules of probably pedogenic origin occur.The base of the overlying Unit V1 is marked by a flooding surface at the base of finely laminated offshore mudsto-nes. These mudstones show a gradual upward increase of organic matter content, accompained by gradual decreasein iron oxides, reflected by a gradual change of colour from red-brown at the base through grey-brown to dark greyat the top. These trends are interpreted as a record of the lake bottom waters# increasing oxygen depletion, whichcould be caused by a rise of lake level and the establishmnet of a stratified water column as well as by an increase inbioproductivity. The overlying anoxic offshore facies probably represents the period of highest lake level with per-manent stratification and high bioproductivity. Beds characterised by alternations of well-defined black clayey lami-nae and white microspar laminae (similar to the anoxic facies of the Kundratice section) are common within thissuccession and are interpreted as reflecting seasonal variations of bioproductivity, sediment imput and water che-mistry. The top of the Unit V1 is a finely laminated nearshore carbonate (Li), which is characterised by alternationsof dark grey, organic matter-rich laminae and red-violet iron oxides pigmented submilimetre-thick laminae. This unu-sual feature can be caused by seasonal/annual changes of bioproductivity and relatively high carbonate accumulation.The presence of amphibian fossils provides evidence of relatively shallow water conditions.The lower part of the overlying Unit V2 is formed by a sandy mudstone slump bed (Fig. 4) overlain by anoxic to suo-xic offshore mudstones (Ml). The upper part of Unit V2 is formed by muddy microbial mat carbonate with mudcracksand pedogenic nodules at the top.

Flora: About 30species of flora (sphenophyts, pterophyts, pteridosperms, cordaits and conifers are known.

Fauna: Conchostracans: Pseudestheria breitenbachensis, Pseudestheria sp.; Pelecypods: ?Anthraconaia sp.; Insects:fragment of the wing; Acanthodians: Acanthodes gracilis; Sharks: Bohemiacanthus carinatus; Actinopterygians:Paramblypterus sp., Amphibia: Melanerpeton sp.; Trails of arthropods: ?Taslerella sp.; Tetrapod footprints: Protrito-nichnites lacertoides.

Stop 4

Locality: Horní Kalná „Dump of the Adam mine“Stratigraphy: Kalná Horizon, Proseãné Formation, Sakmarian.

During the Sakmarian the central part of the Krkono‰e Piedmont basin was occupied by low-relief arid alluvial-lacu-strine sedimentary system, which is recorded by more than 60m thick succesion of red-brown mudstones with rareintercalations of siltstones and fine grained sandstones of the Upper Proseãné Formation. This succession representsalluvial plain facies, which alternate with temporary lake facies. Temporary lake facies include offshore facies, stormdeposits, nearshore carbonates and mudflats. Alluvial plain facies are represented by massive mudstones, tabularbodies of sandstones (sand sheets) and single event scours (small channels) filled by unsorted sandstones. Periods ofnon-sedimentation are recorded by paleosol horizons within alluvial plain mudstones. Frequent facies transitions arerelated to climatically driven lake level fluctuations. The Upper Proseãné Formation contains in the lower part so called Kalná Horizon formed by 10-20m thick packageof grey-black lacustrine mudstone, claystones, carbonates and siltstones (Fig. 7). These deposits represent sedimen-tation in deeper semipermanent lake. Layers of the Kalná Horizon are enriched with Cu-sulfides and they were sub-ject of the mining as in the 19th century as lastly in the years 1949-1952. The dumps after mining with bituminousshales yielded rich fauna and flora (MA≈OUROVÁ 1981, ·TAMBERG 1982, ZAJÍC et al. 1997).

Flora (after ·imÛnek – personal communication): Calamites suckowii, Calamites cf. gigas, Asterophyllites equiseti-formis, Calamostachya germanica, Sphenophyllum sp., Sigillaria sp., Sphenopteris sp., Nemejcopteris feminaefor-mis, Pecopteris cyathea, Pecopteris polypodioides, Pecopteris plumosa, Odontopteris subcrenulata, Neurocallipterisneuropteroides, Neurodontopteris auriculata, Autunia conferta, „Callipteris“ type woldrichii, Walchia piniformis,Culmitzschia laxifolia, Cordaites borassifolius, Cordaites principalis.

Fauna: Conchostracans; Sharks: Xenacanthus decheni; Actinopterygians: Paramblypterus sp., „Amblypterus“ vrati-slaviensis, „Amblypterus“ kablikae, „Amblypterus feistmanteli; Amphibia: Apateon sp.; Coprolites, tetrapod footp-rints.


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Fig. 7. Lithological profile of the outcrop Horní Kalná „Behind garage“. (After Blecha, Martínek & Mihaljeviã 1999).


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BOSKOVICE GRABEN

The Boskovice Graben (Boskovice Furrow, Boskovice Basin) is the name first introduced in 1902 by E. TIETZE for thenarrow depression running south-north from Moravsk˘ Krumlov through Rosice, Boskovice, Letovice as far as Îam-berk. Later HAVLENA (1960) named the northern part of this strip between Kfienov and Îamberk as the Orlice Basin.The name Boskovice Graben in the more restricted sense of HAVLENA (1960) for the narrow depression betweenMoravsk˘ Krumlov and Moravská Tfiebová filled by Upper Carboniferous and Permian sediments is used.Boskovice Graben is based on the line of weakness. It is surrounding with âeskomoravská Highland in the west andBrno Massif in the east. Sedimentation begun in Stephanian C after Asturian movements and it continued without inter-ruption to Lower Permian. The syn-sedimentary movements accompained the infilling of the graben, so about 2000 mthick sedimentary sequence accumulated in narrow depression. The beginning of sedimentation in the graben form con-glomerates and breccias, after sediments are finer. There are two different facies developed in the eastern and westernparts of the Boskovice Graben. Whilst the accumulation in the western part of graben continues with finer sedimentswith coal seams, in the eastern part continue the coarse-grained sediments, and in some places (Rokytná Conglomera-tes) also even through the sedimentation of Permian units.Carboniferous sediments (Stephanian C) are developed in the southern part of the graben only. They are represented byRosice-Oslavany Coal Seams. The lower and middle coal seams have character of Stephanian C, whilst the upper coalseam contains Autunia conferta and is considered to be Lower Autunian (Asselian). The sediments of the Boskovice Graben have been the object of interest to numerous palaeontologists already from themiddle of nineteen century. The palaeontological research proceeded in several periods.We record the first period in the second half of 19th century. It is the time of discovering of first amphibians and acti-nopterygians in the middle and southern regions of the Boskovice Basin (MAKOWSKY 1876, RZEHAK 1881). Prof.J. Augusta is a representative of the second period in the twentieth and thirties last century. He discovered several newpalaeontological sites also in the northern region and collected numerous fauna and flora. The most intensive palaeon-tological excavations proceeded in the fifties and sixties in the northern region of Boskovice Graben. The main objectof interest have been discosauriscids which have been studied by Z. ·pinar and new finds of insects studied by J. Kuka-lová. The last period of the research of Boskovice Graben begun at eighties of the last century and still continue. Thewidespread excavation is proceeded by the staff of the Museum of Eastern Bohemia at Hradec Králové in the northernregion in the vicinity of Letovice and in southern region near by the village Neslovice. The complete references con-cerning paleontology of the Boskovice Basin have been presented ZAJÍC (1997) and recently IVANOV (2003).

Biostratigraphy and correlation of the horizons(after ZAJÍC & ·TAMBERG 2004)

Fossil fauna is known from all regions (from south to north: Moravsk˘ Krumlov, Rosice-Oslavany, Veverská Bít˘‰ka,Malá Lhota, and Letovice) of the Boskovice Basin excepted the terminal ones (Miroslav in the south and Jevíãko in thenorth). However, fauna is also known from the detached southernmost segment near Zöbing in Austria. Sediments ofthe Boskovice Basin are tectonically affected so the originally continuous units are therefore broken up into the smallerblocks. The correlation of numerous separate fossiliferous horizons is moreover complicated by the gradual moving ofthe sedimentation from south to north (Figs. 8, 9). The fauna bearing localities are, however, in some cases not possiblepositively sorted into an existing horizon. The following six stages were erected on the basis of geographic and biostra-tigraphic position:

1) The Rosice-Oslavany Formation – the age is based on flora because the index fossils of the presumable Sphaerole-pis-Elonichthys biozone were not found. The rare remains of Edaphosaurus (Oslavany, coal from the dump of the Kuklamine; PRANTL 1943) and one insect wing of the genus Anthracoblattina (Oslavany, coal seam on the left bank of theriver Oslava; SCHNEIDER 1983) were still discovered regardless of trace fossils. This stage occurs only in the Rosice-Oslavany region.

2). The Padochov Formation – the characteristic lower part of the Acanthodes gracilis biozone (the nominal taxon israther common). The Zb˘‰ov and ¤íãany Horizons are not distinguishable according to faunal content. Both horizonscontain abundant nominal acanthodians Acanthodes gracilis (Beyrich, 1848). Characteristic species of the biozone isalso shark. Tiny teeth of this small piscivorous predator had typically shaped lateral cusps. Teeth of Bohemiacanthus


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carinatus (Fritsch, 1890) were determined from the Zb˘‰ov Horizon (ZAJÍC 1996; ZAJÍC, MARTÍNEK, ·IMÒNEK &DRÁBKOVÁ 1996). ¤íãany Horizon belongs to the Spiloblattina weissigensis biozone (based on insects) because notonly the nominal taxon but also two important accompanying species (Moravamylacris ricanyensis Schneider, 1890 andOpsimylacris procera Haupt, 1952) were found here. This biozone approximately corresponds to the middle phase ofthe Acanthodes gracilis biozone. The same biozone is known from the Lower Goldlauterer Member of the ThüringerWald or from the Maroon Formation in Colorado. SCHNEIDER (1982) parallelized the Spiloblattina weissigensis bio-zone with the Sysciophlebia balteana biozone that is known both from the Lower Goldlauterer Member of the Thürin-ger Wald and the Cassvill Shales (Dunkard Group) of West Virginia.Vertebrates of the Zb˘‰ov Horizon are mostly frag-mentary and affected by hair cracks. The new aeduellid actinopterygian is, however, known only from the ¤íãany Hori-zon up to date. Similar faunal assemblage comes from the Rudník Horizon in the Krkono‰e Piedmont Basin. This stageis known from the Moravsk˘ Krumlov, Rosice-Oslavany, and Veverská Bit˘‰ka regions.

Fig. 8. Lithostratigraphic table of Stephanian and Autunian of the Boskovice Graben (from Pe‰ek et al. 2001). 1-Balinsk˘ conglomerates; 2 – Reddish brown sandstones, siltstones and claystones; 3 – Grey sandstones, siltstones andclaystones with coal seams (I-III) and pelocarbonate horizons 2.1-4.6: 2.1- Zb˘‰ov Hor., 2.2-¤íãany Hor., 3.1-ChudãiceHor., 4.1-Zbraslavec Hor., 4.2-Zbonûk-Svitávka Hor., 4.3-Lubû Hor., 4.4.-Kochov Hor., 4.5-Míchov Hor., 4.6-BaãovHor.; 4-Arcoses; 5- Rokytná conglomerates; 6 – Formations - 1-Rosice-Oslavany Formation, 2-Padochov Formation, 3-Veverská Bit˘‰ka Formation, 4-Letovice Formation; 7- Regions.


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3) The Veverská Bít˘‰ka Formation – any fauna still was notfound.

4) The Lower Letovice Formation – the upper part of theAcanthodes gracilis biozone (the nominal taxon is rather lessfrequent) was found in the Zbraslavec, Zbonûk-Svitávka, andLubû Horizons. The superposition of the horizons is, however,still not validated. The Malá Lhota and Letovice regions yieldfauna of this stage. The upper part of the Acanthodes gracilisbiozone is also affirmed by presence of insect species Syscioph-lebia alligans (nominal taxon of the biozone; defined bySCHNEIDER (1982) from the Boskovice Basin), Opsimylacrissvitaviensis Schneider, 1980 and Moravamylacris sp. Acantho-dian remains are more rare here than in the lower part of the bio-zone. The fossiliferous equivalent was not found in the Krko-no‰e Piedmont Basin up to date. The stratigraphically inappli-cable fauna of the stage comes chiefly from the KozinecHorizon in the Krkono‰e Piedmont Basin. The Kozinec Horizonyields pelecypods Palaeanodonta castor (Eichwald, 1861) anda tetrapod rib (still undescribed find). The exact boundary andrelation between the Acanthodes gracilis and Xenacanthusdecheni biozones are not known. An interdigitation of the bio-zones (in sense of the present definition) is more likely than thesuperposition. Shark remains are (contrary to the Rudník andKalná Horizons of the Krkono‰e Piedmont Basin) extremelyrare. The Zbraslavec, Zbonûk-Svitávka, and Lubû Horizons areundistinguishable according their fauna.

5) The Middle Letovice Formation – the Xenacanthus dechenibiozone was found in the Kochov, Míchov and Baãov Horizonsof the Malá Lhota and Letovice regions. The local horizons arenot recognizable on the basis of fauna and probably representone unit or stratigraphic level. The age of the Xenacanthusdecheni biozone is affirmed by presence of the nominal taxonand by accompanying occurrence of amphibians Discosauris-cus. Discosauriscids are known in Czech Republic (the Bosko-vice Basin, the Intra-Sudetic Basin) only from this biozone. Theinsect species Sysciophlebia alligans evidently pass to the Xena-canthus decheni biozone. The Sysciophlebia alligans biozonethus persists from the upper part of the Acanthodes gracilis bio-zone to the lower part of the Xenacanthus decheni biozone. TheSysciophlebia alligans biozone is also documented by theaccompanying species Opsimylacris svitaviensis Schneider,1980 and Moravamylacris sp. However, the important accom-panying species Xenoblatta ornatissima (Deichmüller, 1887),Sysciophlebia n. sp. and Spiloblattina odernheimensis Schnei-der, 1982 was discovered. Both latter mentioned biozones are ofsimilar extent (SCHNEIDER 1982) and come from the Odern-heim Member of the Saar-Nahe Basin. This stage is possible tocorrelate with the Upper Proseãné Formation in the Krkono‰ePiedmont Basin and with the Upper Olivûtín Member in theIntra-Sudetic Basin.

6) The Upper Member of the Letovice Formation – any faunastill was not found.Fi

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72

Stop 1

Locality: Obora.Stratigraphy: Middle Letovice Formation.

Two main fossiliferous horizons are necessary to distinguish on the locality Obora (Fig. 10). The bottom one (Fig. 11)of claystone famous for rich asseblage of insect (more than 100 species) already formerly described in several papersof KUKALOVÁ. Besides the insect, conchostracans Lioestheria lallyensis Depéret & Mazeran, 1912 also occurs in thisbed. The topmost layer of light - yellow carbonate contains actinopterygians of the genus Paramblypterus and amhibi-ans of the genus Discosauriscus. The nominal taxon of biozone (Xenacanthus decheni) has been described from thislocality already former (ZÍDEK 1966). The poorly preserved skull (17 mm long) of an eryopoid amphibian Dasycepssp. was excavated and described recently DOSTÁL (2003), MILNER, KLEMBARA & DOSTÁL (2007). Lower verte-brates association and their distribution in the bed point to correlation of this horizon with ones on the localities Drvá-lovice „Wind mill“, Kochov „In the streams” and others.

Flora: (after ·imÛnek – personal communication) Annularia stellata, Calamostachys sp, Sphenopteris sp., Pecopteriscf. cyathea, Pecopteris sp., Odontopteris lingulata, Neuropteris cordata, Cyclopteris sp., Arnhardtia scheibei, Autunianaumannii, Taeniopteris jejunata, Cordaites sp., Poacordaites sp., Culmitzschia hirmeri, Culmitzschia parvifolia, Cul-mitzschia speciosa, Ernestiodendron filiciforme, Hermitia arnhardtii, Hermitia germanica, Otovicia hypnoides, Walchiagoeppertiana, Walchia piniformis, Walchia sp., Walchiostrobus sp., Artisia sp., ?Cyclopteris sp., Cordaicarpus isp.

Fig. 10. Sedimentological section measured at Obora. (After Martínek, orig.).


73

Stop 2

Locality: Kladoruby “Dolní pepfiík“Stratigraphy: Lubû or Svitávka Horizon, Middle Letovice Formation.

Probably the Lubû or Svitávka Horizon. Outcrop with various types of claystones, sandstones and carbonates. Locality Kladoruby “Dolní pepfiík” is quite new and up to now research works indicate the differencies from the fossi-liferous horizons outcropping in the vicinity of Kladoruby, Drválovice, Kochov and Baãov. On the basis of the type offauna is older and probably belongs to the Svitávka or Lubû Horizons. The consequence of layers and fauna is differentto horizons on the above mentioned localities. Discosauriscid amphibians, very abundant in the carbonate layer of BaãovHorizon, are limited in the Kladoruby “Dolní pepfiík” to the layer of yellowish-spotted claystone in the bottom part ofthe outcrop (Discosauriscus sp.). Their occurence is relatively rare and specimens are small, not exceeding 15 cm of thetotal length. The actinopterygians are not numerous, but laminated claystones and limestones offered quite new genusand species of actinopterygians, unknowns from another permian localities of the Bohemian Massif (·TAMBERG2007). The new genus Letovichthys with species L. tuberculatus ·tamberg, 2007 and L. multidentatus ·tamberg, 2007was described, on the other hand, the genus Paramblypterus, which is very abundant at other localities of the northernregion of Boskovice Graben or members of the family Aeduellidae are absolutely missing. The cardial feature of thisoutcrop is abundant occurrence of acanthodians. The most numerous findings are represented by Acanthodes gracilis(Beyrich, 1848) and new species Acanthodes stambergi Zajíc, 2005. Fragments of a xenacanthid shark are known.Fossiliferous claystones deposit probably in somewhat different environment than the carbonate layer and fish beds ofthe Baãov Horizon. The abundant ferns and gymnosperms occur in the locality. Some fans of leaves are of about 50 cmlong. This feature together with rare of actinopterygians assumed the contiguity of lakeshore.

Flora (after ·imÛnek – personal communication): Annularia cf. mucronata, Asterophyllites equisetiformis, Pecopteriscyathea, Aphlebia sp., Odontopteris subcrenulata, Neurodontopteris auriculata, Neuropteris sp., Autunia conferta, Autu-nia naumannii, Dichophyllum cf. flabelliferum, Gracilopteris bergeronii, Rhachiphyllum schenkii, „Callipteris“ sp.,Taeniopteris sp., Cordaites sp., Poacordaites sp., Culnitzschia frondosa var. Zeilleri, Culmitzschia parvifolia, Culmitzs-chia speciosa, Ernestiodendron filiciforme, Hermitia schlotheimii, Otovicia hypnoides, Walchia goeppertiana, Walchiapiniformis, Walchia nov. sp., Walchia sp., Gomphostrobus bifidus.

Fig. 11. Locality Obora. Horizon with insect in the bottom of theoutcrop.


74

Fig. 12. Sequence of beds in the eastern part ofthe outcrop Kladoruby „Dolní pepfiík“. (After·tamberg 2007).Layer 1. Grey claystone with flora. Layer2.Thickness 5 cm.Laminated bituminous car-bonate with thin yellowish lamina. Fossil con-

tent comprised of large leaves of flora, isolated bones and fragments of discosauriscid skeletons, and spines and frag-ments of Acanthodes.Layer 3.Thickness 0.5 cm. Light grey claystone with abundant debris of flora. Layer 4. Thickness7 cm. Grey claystone with flora, does not split into slabs. Layer 5. Thickness 6 cm. Yellow decaying sandstone. Layer6. Thickness 13 cm. Yellowish grey silty claystone with debris of flora, does not split into slabs. Layer 7. Thickness 8cm. Greyish green claystone with Acanthodes and abundant flora. Layer 8. Thickness 30 cm. Finely laminated clayeylimestone with acanthodians, xenacanthids, actinopterygians and flora. Layer 9. Thickness 2.5 cm. Yellow and greensandstone without fossils. Thickens to 4 cm in its western extension. Layer 10. Thickness 12 cm. Grey claystone withacanthodians, xenacanthids, actinopterygians, and abundant flora. Layer 11. Thickness 13 cm. Yellow sandstone withclayey admixture. Layer 12. Thickness 50 cm. Grey or greyish green claystone with vertical roots, abundant debris offlora, and rare acnthodians and actinopterygians. Layer 13. Grey massive sandstone.

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Fig. 13. Comparison of the sequ-ence of the beds recorded on thelocality Kochov „In the streams“,Kochov „Horka“ and Drválovice„Windmill“. The sequence ofmost important fossiliferous layerof limestone with discosauriscidamphibians and actinopterygiansand overlying laminated calcare-ous claystone with abundant acti-nopterygians are marked on allthree profiles. A – Sequence ofbeds on southern part of theKochov „In the stream“ locality;B – Sequence of beds on theKochov „Horka“ locality; C –Sequence of the beds on theDrválovice „Windmill“ locality.See legend on the Fig. 12. (After·tamberg 2007).


76

Stop 3 and 4

Localities: Baãov „Na Skalkách quarry“, Sudice = Baãov II (uncompleted motorway cut)Stratigraphy: Baãov Horizon; Middle Letovice Formation.

The both outcrops represent the Middle Gray Baãov Beds (HAVLENA & ·PINAR 1956). Deposits contain a key hori-zon of gray pelocarbonate shales in which there are abundant flora and very numerous skeletal remains of discosauris-cids and actinopterygians. The fauna is accompained by the usual Lower Permian flora, of which large fans are oftenpreserved. The thicknes of the bituminous layer is of about 28 cm and varies only slightly. The skeletons of discosau-riscids and actinopterygians are carbonised. The similar layer with the same thickness and the fossil contents outcropson several localities 5 km north of Baãov (Fig. 12). The difference is only in the type of fossilisation, the skeletons arefossilised by calcium phosphate.

Flora: Calamites cf. gigas, Calamites sp., Annularia sphenophylloides, Annularia spicata, Annularia stellata, Asterop-hyllites longifolius, Calamostachys sp., Sphenophyllum thonii, Sphenopteris sp., Pecopteris arborescens, Pecopteriscyathea, Pecopteris hemitellioides, Pecopteris plumosa, Pecopteris sp., Aphlebia sp., Metacalamostachys dumasii,Calamostachys sp. , Pecopteris arborescens, Pecopteris cyathea, Pecopteris hemitellioides, Pecopteris plumosa, Peco-pteris sp., Alethopteris sp., Odontopteris lingulata, Odontopteris subcrenulata, Odontopteris sp., Neuropteris sp., Arn-hardtia cf. scheibei, Autunia conferta, Gracilopteris cf. bergeronnii, Rhachiphallum lyratifolia, Peltaspermum sp., Tae-niopteris multiramis, Taeniopteris jejunata, Taeniopteris sp., Cordaites palmaeformis, Cordaites principalis, Cordaitessp., Poacordaites sp., Dicranophyllum longifolium, Culmitzschia frondosa var. Zeilleri, Culmitzschia parvifolia, Cul-mitzschia speciosa, Ernestiodendron filiciforme, Hermitia germanica , Hermitia rigidula, Otovicia hypnoides, Walchiagoeppertiana, Walchia piniformis, Walchia sp., Artisia sp., Cyclopteris sp., Carpentieria marocana, ?Cardiocarpus sp.,Cordaicarpus sp., Samaropsis sp.

Fauna: Conchostracans; Sharks: Xenacanthus sp.; Actinopterygians: Paramblypterus sp.; Amphibia: Discosauriscusaustriacus, Discosauriscus pulcherrimus

References

BLECHA, M. et al. (1997): Zmûny prostfiedí na rozhraní karbonua permu a jejich dopad na spoleãenstva organismÛ ve fosili-ferních obzorech podkrkono‰ské pánve. - Závûreãná zpráva zagrant GA âR, Ústfiední Ústav geologick˘, MS, 1-177. Praha.

BLECHA, M., MARTÍNEK, K. & MIHALJEVIâ, M. (1999):Paleoenvironmental changes of the semipermanent KalnáLake (Lower Permian), Krkono‰e Piedmont Basin, CzechRepublic: sedimentary and geochemical record. – Acta Uni-versitatis Carolinae, Geologica, 43, 4, 657-665. Praha.

DOSTÁL, O. (2003): Zástupci ãeledi Discosauriscidae (ROMER1947) na lokalitû Obora. – Geologické v˘zkumy na Moravû ave Slezsku v roce 2002, 10, 40-43. Brno.

FRIâ, A. (1912): Studien im Gebiete der Permformation Böh-mens. – Archiv für die naturwissenschaftliche Landesdurch-forschung Böhmens, 15, 2, 1-52. Prag.

FRITSCH, A. (1879-1901): Fauna der Gaskohle und der Kalkste-ine der Permformation Böhmens. Band 1-4. - F. ¤ivnáã. Prag.

HAVLENA, V. (1960): Nové poznatky z geologie Boskovickébrázdy. – Geologick˘ prÛzkum, 1960, 3, 67-71.

HAVLENA, V. & ·PINAR, Z. V. (1956): Stratigrafie permsk˘chuloÏenin v území mezi Baãovem a Svitávkou na Moravû. -Sborník Ústfiedního ústavu geologického, Oddíl paleontolo-gick˘, 22 (1955), 7-47. Praha.

Fig. 14. Upper part of the Baãov quarry.


77

HECKEL, W. J. (1861): Neue Beiträge zur Kenntniss der fossilen Fische Österreichs. – Denkschriften der mathematisch-naturwissenschaftlichen Classe, 19, 49-63. Wien.

IVANOV, M. (2003): Pfiehled historie paleontologického bádání v permokarbonu boskovické brázdy na Moravû. – ActaMusei Moraviae, Scientiae geologicae, 58 (2003), 3-112. Brno.

MAKOWSKY, A. (1876): Über einen neuen Labyrinthodonten „Archegosaurus austriacus nov. spec.“. – Sitzungsbe-richte der Kaiserlichen Akademie der Wissenschaften. Mathematisch-Naturwissenschaftliche Klasse, 73, 155-166.Wien.

MA≈OUROVÁ, M. (1981): Nov˘ nález branchiosaurÛ na lokalitû Horní Kalná u Vrchlabí. - âasopis Národního Muzea,fiada pfiírodovûdná, 150, 3/4, 169-172. Praha.

MARTÍNEK, K., BLECHA, M., DANùK, V., FRANCÒ, J., HLADÍKOVÁ, J., JOHNOVÁ, R. & ULIâN ,̄ D. (2005):Record of palaeoenvironmental changes in a Lower Permian organic-rich lacustrine succession: Integrated sedimen-tological and geochemical study of the Rudník member, Krkono‰e Piedmont Basin, Czech Republic. - Palaeogeo-graphy, Palaeoclimatology, Palaeoecology, 230, 85-128.

MILNER, A. R., KLEMBARA, J. & DOSTÁL, O. (2007): A zatrachydid temnospondyl from the Lower Permian of theBoskovice Furrow in Moravia (Czech Republic). – Journal of Vertebrate Paleontology, 27, 3, 711-715.

TÁSLER, R., HAVLENA, V. & PROUZA, V. (1981): Nové litostratigrafické ãlenûní centrální a západní ãásti podkrko-no‰ské pánve. Vûstník Ústfiedního ústavu geologického, 56, 129-143. Praha.

PE·EK, J. et al. (2001): Geologie a loÏiska svrchnopaleozoick˘ch limnick˘ch pánví âeské republiky. – âesk˘ geolo-gick˘ ústav, 1-243. Praha.

PRANTL, F. (1943): Vzácn˘ nález v moravském permokarbonu. - Vûda pfiírodní, 22, 4, 93-97. Praha.RIEGER, Z. (1968): Fytopaleontologicko-stratigrafick˘ v˘zkum stefanu a autunu podkrkono‰ské pánve. – Vûstník

ústfiedního ústavu geologického, 43, 6, 449-457. Praha.RZEHAK, A. (1881): Die Fauna des mährischen Rothliegenden. – Verhandlungen der Kaiserl.-Königl. geologischen

Reichsanstalt Vienna, 1881, 78-79. Wien.SCHNEIDER, J. (1982): Entwurf eines biostratigraphischen Zonengliederung mittels der Spiloblattinidae (Blattodea,

Insecta) für das kontinentale euramerische Permokarbon. - Freiberger Forschungshefte, C 375, 27-47. Leipzig.SCHNEIDER, J. (1983): Die Blattodea (Insecta) des Paläozoikums. Teil I: Systematik, Ökologie und Biostratigraphie. -

Freiberger Forschungshefte, C 382, 106-145.·TAMBERG, S. (1982): V̆ sledky paleontologick˘ch v˘zkumÛ na lokalitû Horní Kalná v podkrkono‰ské pánvi. - Acta

Musei Reginaehradecensis S. A., 17, 5-51. Hradec Králové.·TAMBERG, S. (2007): Permo-Carboniferous Actinopterygians of the Boskovice Graben. Part 1. Neslovicella, Bour-

bonnella, Letovichthys, Elonichthys. – Muzeum v˘chodních âech v Hradci Králové, 1-155.ZAJÍC, J. (1997): Zoopaleontologie limnického permokarbonu Boskovické brázdy - souãasn˘ stav v˘zkumu. - Geolo-

gické v˘zkumy na Moravû a ve Slezsku, 4, 85-89. Brno.ZAJÍC, J. (2005): Permian acanthodians of the Czech Republic. - Czech Geological Survey Special Papers, 18, 1-42.

Praha.ZAJÍC, J. (2007): Carboniferous Fauna of the Krkono‰e Piedmont Basin. - Acta Musei reginaehradecensis, Ser. A, 32,

11-16. Hradec Králové.ZAJÍC, J., ·IMÒNEK, Z. & DRÁBKOVÁ, J. (1997): The fossil fauna, mega- and microflora of the Krkono‰e Piedmont

Basin. - Prace Paƒstwowego Instytutu Geologicznego, 157, 197-206. Kraków.ZAJÍC, J. & ·TAMBERG, S. (2004): Selected important fossiliferous horizons of the Boskovice Basin in the light of

the new zoopaleontological data. - Acta Musei Reginaehradecensis, S. A, 30, 5-15. Hradec Králové.

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