Late Devonian-Early Carboniferous Foraminiferal

Geologia 39

Jirl Kalvoda

Late Devonian-Early Carboniferous Foraminiferal Fauna: Zonations, Evolutionary Events, Paleobiogeography and Tectonic Implications

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Masary k U ni versi ty Brno, Czech Republic, 2002

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FOLIA

FACULTATIS SCIENTIARUM NATURALIUlVI UNIVERSITATIS lVIASARYKIAN AE BRUNENSIS

EDITORIAL BOARD: Rudolf Brazdil - geography Rostislav Brzobohaty - geology Josef Havel - chemistry Josef Humlicek - physics, editor-in-chief Ladislav Skula - mathematics Jaromir Vaiihara - biology Jaromir Vosmansky - managing editor

Published by Masaryk University FOLIA, Masaryk University, Faculty of Science, Kotlafskl:i 2,61137, BRNO, Czech Republic, fax: 420541211214, e-Illail:[email protected],[email protected]

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Late Devonian-Early Carboniferous Foraminiferal Fauna: Zonations, Evolutionary Events, Paleobiogeography and Tectonic Implications

Jifi Kalvoda Department of Geology and Paleontology, Masaryk University, Kotlarska 2, 611 37 Brno, Czech Republic

Masaryk University Brna, Czech Republic, 2002

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FOLIA

FACULTATIS SCIENTIARIUM NATURALIUM UNIVERSITATIS MASARYKIANAE BRUNENSIS

Cover drawing: Bradyina rotula

(EICHWALD),

Early Carboniferous

Reviewers:

Jindrich Hladil Institute of Geology, Academy of Sciences of the Czech Republic, Rozvojova 135, 16502 Praha 6-Lysolaje

Petr Storch Institute of Geology, Academy of Sciences of the Czech Republic, Rozvojova 135, 16502 Praha 6-Lysolaje

Type-setting: Rostislav Melichar, system I¥fEX

"©

Jii'l Kalvoda, 2002 ISBN 80-210-2931-5

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Contents 1

Introduction

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Review of Late Devonian-Early Carboniferous Foraminiferal Zonations 11 2.1 East European Platform and the Ural 11 2.2 Western Europe. 16 2.3 Central Europe . . . . 19 20 2.4 Central Asia. . . . . . 2.5 Iran and Afghanistan. 22 2.6 Western Siberia . . . . 22 2.7 The Central Part of Siberia 22 2.8 NE Siberia-Kolyma and Omolon Massifs 32 2.9 North America . . . . . . . . . . . . . . 34

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Late Devonian-Early Carboniferous Foraminiferal Zonation in Moravia 37 3.1 Introduction........................... 37 3.2 Geology and Paleozoic Sediments of the Brunovistulian Terrane 37 41 3.3 Foraminiferal Zonation . . . . . . . . . . . . 3.3.1 Nanicella uralica Interval Zone . . . 41 3.3.2 Multiseptida corallina Interval Zone 43· 3.3.3 Eonodosaria evlanensis Range Zone 44 3.3.4 Eonodosaria evlanensis-Quasiendothyra communis Interzone . . . . . . . . . . . . . . . . . . . . . . . . . 45 3.3.5 Quasiendothyra communis-Quasiendothyra regularis Interval Zone . . . . . . . . . . . . . . . . . . . . .. 46 3.3.6 Quasiendothyra kobeitusana-Quasiendothyra konen47 sis Interval Zone . . . . . . . . . . . . . . 48 3.3.7 Tournayellina beata Interval Zone 50 3.3.8 Chernyshinella glomiformis Interval Zone 3.3.9 Chernyshinella tumulosa-Spinobrunsiina Interval Zone 50 3.3.10 Paraendothyra Interval Zone . . . . . . . . . 51 3.3.11 Tetrataxis-Eotextularia diversa Interval Zone . . .. 53 3.3.12 Eoparastaffella simplex Interval Zone . . . . . . . . 55 3.3.13 Viseidiscus eospirillinoides-Glomodiscus oblongus Interval Zone. . . . . . . . . . . . . . . . . 57 3.3.14 Pojarkovella nibelis Interval Zone. . . . . . . . . .. 58

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3.3.15 Neoarchaediscus Interval Zone . . . . . . . . . . . . 3.3.16 Loeblichia paraammonoides-Asteroarchaediscus Interval Zone. . . . . . . . . . . . . . . . . . . . . . . .. 4 Relation of the Moravian Zonation to Other D-C Zonations 4.1 Introduction........................... 4.2 Correlation of the Most Important Foraminiferal Zonations 4.3 Development of the Attitudes to the Early Carboniferous Subdivision . . . . . . . . . . . . . . . . . . . . . . . . . ..

59 62 63

63 64 70

5 Late Devonian-Early Carboniferous Foraminiferal Dispersal 81 5.1 Introduction................... 81 5.2 Paleobiogeography . . . . . . . . . . . . . . . . 82 5.3 The Evolution of the Foraminiferal Dispersal 94 5.3.1 Introduction 94 95 5.3.2 Late Devonian . . . 97 5.3.3 Early Carboniferous 6 D-C Foraminiferal Fauna, Eustacy and Climatic Oscillations 103 6.1 Introduction.................... 103 6.2 Late Frasnian and Frasnian/Famennian Event . 104 6.3 Early and Middle Famennian . . . . . . . . . . 107 6.4 Late Famennian and Devonian/Carboniferous Events. . 108 6.5 Early Tournaisian. . . . . . . . . . . . . . . . . . . . . 112 6.6 Middle Tournaisian and the Middle/Late Tournaisian Boundary Event . . . . . . . . . . . . . . . . . . . . . . . . . . . 114 6.7 Late Tournaisian and Tournaisian/Visean Boundary Interval 116 6.8 Rest of the Visean .. . . . 117 6.9 Discussion and Conclusions . . . . . . . . . . . . . . . . .. 118 7 D-C Foraminiferal Paleobiogeography and Perigondwana Terranes 121 7.1 Introduction........................... 121 7.2 Caledonian and Variscan Terranes at the SE Margin of Lau121 russia . . . . . . . . . . . . . . . 124 7.3 Geological Setting . . . . . . . . 124 7.3.1 SE Margin of Laurussia

7.4

7.5

7.3.2 Central Asia . . . . . . . . . . . . . . . Paleobiogeography . . . . . . . . . . . . . . . . 7.4.1 Central European and Moesian terranes 7.4.2 Istanbul Zone . . . . . . . . . . . . . . . 7.4.3 Blocks in Karakaya Complex . . . . . . 7.4.4 Nappe Units of the Northern Part of the AnatolideTauride Zone 7.4.5 Elburz........ 7.4.6 Afghanistan..... Discussion and Conclusions 7.5.1 Turkey.... 7.5.2 Iran . . . . . 7.5.3 Afghanistan..

130 134 134 134 135 136 139 142 144 144 150 151

8

Summary

155

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References

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List of Figures 1 2 3 4 5 6 7 8 9 10 11 12 13 14

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Com parison of some early zonations in the Eastern Europe Early Carboniferous foraminiferal zonation . . . . . . . . . Late Devonian-early Carboniferous foraminiferal zonation with typical index taxa . . . . . . . . . . . . . . . . . . . . . Foraminiferal zonation of late Tournaisian-early Visean. .. Latest Tournaisian-Visean foraminiferal zonation . . . . .. Latest Devonian-early Carboniferous foraminiferal zones with typical taxa in Western Europe . . . . . . . . . . . . . . .. Com parison of latest Devonian-early Carboniferous zonations in Central Asia . . . . . . . . . . . . . . . . . . . . .. Early Carboniferous foraminiferal zonation of southern Kazakhstan . . . . . . . . . . . . . . . . . . . . . . . . . . . .. Foraminiferal zonation of West Siberian Platform correlated with the Ural and East European Platform . . . . . . . . . Early Carboniferous foraminiferal zonation of equatorial and northern latitude belt . . . . . . . . . . . . . . . . . . . . . Correlation of Devonian foraminiferal zones in the West Siberian Platform and the Kuznets Basin . . . . . . . . . . . Correlation of Devonian foraminiferal zones in the Western and Eastern Ural . . . . . . . . . . . . . . . . . . . . . . .. Correlation of foraminiferal zones in Western Europe with foraminiferal zones in the Omolon Massif . . . . . . . . . . Correlation of the foraminiferal zonation of Zeller (1957) with foraminiferal zonation of Woodland (1958) and McKay and Green (1963) . . . . . . . . . . . . . . . . . . . . . . .. Early Carboniferous foraminiferal zones and ranges of taxa in Arizona. . . . . . . . . . . . . . . . . . . . . . . . . . .. Correlation of North American foraminiferal zonatio~s with Eastern Europe . . . . . . . . . . . . . . . . . . . . . . . .. Sim plified geological map of Moravia with the location of three major pre-flysch developments . . . . . . . . . . . .. Correlation of the Paleozoic pre-flysch sedimentation in central and SE Moravia . . . . . . . . . . . . . . . . . . . . .. Map of discussed localities and boreholes in Moravia . . .. Late Tournaisian-early Visean foraminiferal zones in Moravia (Czech Republic) and correlation with conodont zonation and major eustatic oscillations . . . . . . . . . . . . . . . .

13 14 15 16 17 18 21 23 24 25 26 27 28

29 31 33 38 39 42

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31 32 33 34 35 36

Distribution of the genera Eoparastaffella and Eoendothyranopsis in the Tn/V boundary interval in the Mokra quarry near Brno . . . . ... . Stratigraphical ranges of important foraminiferal taxa in Moravia in the late Devonian-middle Tournaisian . Stratigraphical ranges of important foraminiferal taxa in Mo.. ravia in late Tournaisian and Visean Correlation chart of important late Devonian-early Carboniferous foraminiferal zonations Correlation chart of middle and late Devonian zonations in Moravia. . . . . . . .. .. Correlation of the late Devonian-early Carboniferous foraminiferal, conodont and ammonoid zonation .

56 60 61 65 67 69

Correlation of different levels of the Tournaisian/Visean boundary in the stratotype profile in Bastion near Dinant and il! Salet . . . . . . ... . . . . . . . . . 71 Morphotypes of the genus Eoparastaffella and their stratigraphic distribution .. 77 Correlation of foraminiferal associations in the transitional beds between Tournaisian and Visean in Guangxi (southern China) and Belgium ... .. .. 78 Early Carboniferous paleogeographic scheme illustrating the location of the North Paleotethyan, Siberian, North American and Perigondana realms . . . . . . . 82 Localization of different regions in Siberia discussed in the text .. . . . .. .. .. ... . . . 84 Schematic geologic map of NE Siberia . . . . 86 Tectonic model of the Russian Far East, Alaska and northern part of the Canadian Cordillera in Early Carboniferous 87 Scheme showing the location of Cimmerian terranes in SE Asia .. . . . . . . . .. .. 93 Scheme showing the distribution of some important foraminiferal genera in late Devonian . . . . 104 Scheme showing migration of North Paleotethyan foraminiferal fauna and inferred climatic oscillations in late Devonian 109 and early Carboniferous . . . . .

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Eustatic oscillations, major lithological changes and foraminiferal, cephalopod, conodont zonations in the late Famennian and early Tournaisian . . . . . . . . . . . . . . . . . . 111 Generalized correlation of foraminiferal, conodont and lithological cycles and climatic episodes at the Middle/Late Tournaisian boundary . . . . . . . . . . . . . . . . . . . . . . .. 115 Sketch of the microcontinents in the Central European Variscides. . . . . . . . . . . . . . . . . . . . . . . . . . . 122 Structural setting of the Brunovistulian, Malopolska and Lysogory terranes. . . . . . . . . . . . . . . . . . . . . . .. 126 Tectonic map of Turkey and surrounding areas with the situation of major terranes discussed in the article . . . . .. 128 Location of major tectonic blocks of western Central Asia . 131 Location of terranes in Afghanistan. . . . . . . . . . . . .. 132 Sketch showing the relationship between blocks at the northern margin of the Indian Subcontinent in Permian . . . . . 133 One of the possible scenarios for the late Carboniferous paleogeography of the Istanbul, Sakarya and North AnatolideTauride terranes . . . . . . . . . . . . . . . . . . . . . . . . 147 Early Carboniferous paleogeographic reconstruction with alternative positions of the Sakarya and North Anatolide-Tau ride terranes . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 148

List of Tables 1

List of Cadomian terranes in Central and Southeastern Eu~ope and Asia Minor

124

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1

Introduction

The study of late Devonian and early Carboniferous calcareous foraminifers had already begun by the mid-nineteenth century. The first papers on Carboniferous foraminifers are by Ehrenberg (1843,1854) and Eichwald (1860). The following papers by Brady (1873, 1873a) and Moeller (1878, 1879) had already a relatively high standard and the species described by them remain valid, they did not immediately result in further research. This was primarily due to the fact that finds of isolated forms of calcareous foraminifers are relatively rare. For this reason further development of their study required a new methodological approach. This new approach-research on the basis of using only thin sectioned material was closely connected with the development of oil-prospecting in the former Soviet Union in the period before and during World War II, and it is inseparably connected with the Professor Rauser-Chernousova. She collected a team of researchers in the 1940s who, together, laid the foundation for the biostratigraphic utilisation of calcareous foraminifers. A considerable part of information remained, however, only in manuscripts during the war years and it was published only in 1948 in what has already become a classic monograph (RauserChernousova et al., 1948). Investigations into the biostratigraphic utilisation of calcareous foraminifers of the late Devonian and the early Carboniferous in the former Soviet Union thus preceded investigations in other parts of the world. Calcareous foraminifers were first used for the stratigraphic characterization of lithological horizons together with other groups of the fauna. Further development of systematic studies as well as a rapid growth of the knowledge of stratigraphic distribution of calcareous foraminifers led in the 1960s to the formation of the first foraminiferal zonations in several papers by ' E. Reitlinger, O. Lipina, N. Brazhnikova and M. Vdovenko. In Western Europe and North America, the more extensive biostratigraphic ~tilization of the foraminiferal fauna started in the 1970s in pioneering papers by Bernard Mamet, Betty Skipp, Raphael Conil and Maurice Lys and, very soon calcareous foraminifers became an important tool for biostratigraphy also here. Towards the end of the twentieth century, foraminiferal fauna has been applied increasingly for biostratigraphy also in Central Europe, SW, SE and E Asia, North Africa and the growing amount of data contributed to its increasing importance in paleobiogeographic interpretations.

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1 Introduction

The aims of this monograph are: 1. to provide a brief review of the most important foraminiferal zona-

2.

3. 4. 5. 6.

tions, present a late Devonian-early Carboniferous foraminiferal zonation in Moravia where some key profiles enable a good correlation with conodont zonation to present a correlation of the zones established in Moravia with other important zonations in all paleobiogeographic realms to review main events in the evolution of foraminiferal fauna and their relation to eustacy and climatic oscillations to discuss late Devonian-early Carboniferous foraminiferal paleobiogeography and dispersal in relation to plate tectonics to discuss the impact of foraminiferal paleobiogeography on plate tectonic reconstructions at the SE margin of Laurussia and in SW Asia.

The creation of a zonation and paleobiogeographic study always raises the question of applied systematic approaches. It is beyond the scope of this paper to discuss the intriguing state of the taxonomy of late Devonian and early Carboniferous calcareous foraminifers. Many synonymous taxa, definitions based often either on equatorial or axial sections or on not fully diagnostic sections, a poor knowledge of variability and the poor quality of many illustrations constitute only a part of wide range of problems whose solution will require decades of systematic work including teams of workers. At the generic level, the present paper especially builds on the recent study of Rauser et al. (1996) and latest work on dainellids by Cozar and Vachard (2001), further information on the systematic approaches can be found in the chapter "Late Devonian-early Carboniferous zonation in Moravia" . Generally it can be stressed that at the species level, only taxa whose systematics is a matter of wider consensus have been applied both in the biostratigraphic and the paleobiogeographic studies. In order to save space, the names of authors of species are given -only where it is of vital importance, i.e. in the chapter on the definition of foraminiferal zones in Moravia and are absent in chapters dealing with the events, correlations and paleobiogeography. As the chapter on foraminiferal zonation in Moravia represents an update of the zonation of Kalvoda (1990), it is only referred to- the figures of stratigraphically important taxa presented here.

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2.1

Review of Late Devonian-Early Carboniferous Foraminiferal Zonations East European Platform and the Ural

In the former USSR the foraminifers have been mostly utilized for the definitions of so-called "horizons". The first foraminiferal zones were singled out in the boundary beds of Devonian and Carboniferous. In the Volga-Ural. region and on the western slopes of the Urals, Lipina (1955) defined the Septatournayella rauserae Zone and a zone "with frequent Quasiendothyra communis". In the western part of the East European Platform, Brazhnikova (Brazhnikova et al., 1956) defined the Eoendothyranopsis stalfelliformis, Lituotubella-H aplophragnella, Forschiella- M onotaxis- Valvulinella and Saccaminopsis zones in the upper part of early Carboniferous. Durkina (1959, 1962) distinguishes in the Timano-Pechora region "beds with Septatournayella rauserae", "beds with Quasiendothyra communis", "beds with Quasiendothyra kobeitusana" and "beds with Septatournayella njumolga" for the boundary horizons of the Devonian and Carboniferous. Malachova (1959) describes in the Tournaisian "beds with Chernyshinella glomiformis" and "beds with Paraendothyra nalivkini and Eoendothyranopsis transita". The first foraminiferal zones for the early Carboniferous and a part of the late Devonian were defined for the territory of the USSR by Reitlinger (1960; see Fig. 1). Lipina (1962) somewhat modified her own zonation of boundary beds of the Devonian and the Carboniferous, when, instead of a zone with frequent Quasiendothyra communis, she singles out the Quasiendothyra kobeitusana Zone. Reitlinger (1964) refined her own earlier biostratigraphical zonation and for the latest Devonian and early Carboniferous, she distinguished thirteen zones (see Fig. 1). A somewhat different zonal scheme can be found in Lipina (1964). In the late Famennian and the Tournaisian the author mentions three globally distributed zones: the Quasiendothyra-Septaglomospiranella-Granuliferella Zone, the Chernyshinella Zone and the Plectogyra Zone. Within the territory of the former USSR she subdivided these three into the following smaller zones: the Septatournayella rauserae Zone, the Quasiendothyra kobeitusana Zone, a zone of unilocular foraminifers, the Chernyshinella ex gr. glomiformisSeptaglomospiranella Zone, the Chernyshinella glomiformis-Palaeospiroplectammina tchernyshinensis Zone, the Tournayella-Spinoendothyra cos-

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2 Review of Late Devonian-Early Carboniferous Foraminiferal Zonations

ti/era Zone, the Eotextularia diversa and Dainella chomatica Zone. Reitlinger (1965) distinguishes in Tournaisian t,hree zones with broad regional distribution: the Chernyshinella, Spinoendothyra and Dainella chomaticaMediocris mediocris zones. The two authors most frequently mentioned here-Lipina and Reitlinger (1970) joined their efforts and defined for the latest Devonian and the early Carboniferous eleven universal regional zones that, with minor modifications, are still being used up today. This zonation, with some modifications carried out by Lipina (1973 and 1979), is given in Figs. 3 and 4. These Eastern European zonations are very important because of rich data on calcareous foraminifers on which they are based on. Their disadvantage is, however, in the fact that the boundaries of the defined zones often coincide with the boundaries of the traditional Russian horizons. The horizons are defined on the basis of lithologic and biostratigraphic data of several faunal groups and it is apparent that the zonal boundaries defined on the basis of different faunal groups may not coincide. The Quasiendothyra kobeitusana-Septaglomospiranella primae va Zone must be, in accordance with the currently valid definition of the Devonian/Carboniferous boundary on the basis of the entry of Siphonodella sulcata, considered to be late Famennian for the most part. The Chernyshinella -Septabrunsiina krainica Zone covers a relatively large time interval of the early and middle Tournaisian, which permits the present knowledge of the calcareous foraminiferal fauna to be specified in considerably greater detail. Its limits, however, have not been very well defined and distinguishing them is practically impossible in the boundary intervals. Dainella chomatica, currently one of the index species in the Dainella chomatica-Eoendothyranopsis transita Zone, already occurs with the species of the preceding zone and the species Eoendothyranopsis transita is not widely distributed. This most probably led Lipina (1973) to rename this zone as the EoparastaffellaO -Eoendothyranopsis Zone. Relatively few problems seem to be connected with further Visean zones. This may to a certain extent reflect the fact that foraminiferal zones in that time interval permit the most detailed stratigraphic subdivision. Conodont zonation in the Visean is much rougher and independent checking is thus missing. In the Dnieper-Donets Basin, Brazhnikova and Vdovenko (1971) assigns the Dainella micula, Eoparastaffella simplex, Uralodiscus rotundusPropermodiscus, Viseiscus eospirillinoides and Lituotubella magna zones to the upper part of the early Carboniferous. This zonation is extended and

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2.1 East European Platform and the Ural

O.A. Lipina 1955-1960

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N.P.Malakhova 1958

E.A. Reitlinger 1960

E.A. Reitlinger 1961-1963

Millerella E08taffella

N

t,)"(.)

g

rg

E08taffella protvae

!t.l/2 ~ .......................... ~ a.ll1 Plectogyra kirgisana

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E08taffella decurta ......................... .

Janlschewskina Eostaffella Ikensls Endothyranopsls Eostaffe/la

Eostffella proikensis

Endothyranopsis compressus Lltuotubella

.... !J(~~p!f!?i.c!~~ .... Urbanella miranda PIectogyra similis

Urbanella vera Paraarchaediscus

Eostaffella nalivkini Endothyra transita Plectogyra

Dainslla chomatica E08taffella mediocris

Plectogyra tuberculata

Spinoendothyra costifera

Chemyshinella

Spinoendothyra tuberculata Chemyshinella glomiformis

Quasiendothyra communis

Quasiandothyra kobeitusana Quas/endothyra konensls

Septaglomospiranella primaeva

Quasiendothyra communis

tuberculata 1------+ .............................................................. .

=(.)

Chemyshinella glomiformis Quas/endothyra communis Q. kobeitusana

Septatoumayella rausarae

Quasiendothyra bella Septaglomosplranella nana

Figure 1: Comparison of some early zonations in the Eastern Europe. Modified according to Reitlinger (1964).

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STAGE

FORAMINIFERAL ZONE Eostaffel/a tenebrosa Eostaffel/a ikensis

c:

co Q)

Archaediscus gigas-Eostaffella proikensis

t/)

:>

Endothyranopsis compressa Planodiscus primaevus-Permodiscus rotundus Dainella chomatica-Eoendothyranopsis transita Endothyra e/egia

c:

Spinoendothyra

·mc:

Endothyra tuberculata

co ·w ':::J

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Chernyshinella-Septabrunsiina krainica Quasiendothyra kobeitusana

Figure 2: Early Carboniferous foraminiferal zonation by Lipina & Reitlinger (1970).

modified by Vdovenko (1973; see Fig. 2.1), who distinguishes one zone in the latest Tournaisian and eight zones in the Visean. For the southern part of the Odessa region and the Moesian Platform, Vdovenko (1974) creates in the Visean the Eoparastaffella-Dainella chomatica, Archaediscus krestovnikovi-Endothyranopsis compressus, Eostaffella proikensis -Archaediscus gigas and Euxinita efremovi -Endostaffella parva Zones. In addition, Vdovenko etal. (1981) create the Spinoendotkyra Zone in the Tournaisian. Of principal importance for the zonation of Visean is a paper by Vdovenko (1980), where the author classifies five global zones and carries out an extensive correlation. The zones of Vdovenko are to a great extent similar to those of Lipina and Reitlinger, but the use of different index species may be a matter of some debate. The choice of the genus Propermodiscus instead of the species Viseidiscus primaevus narrows the facies applicability of the zone and the species Lituotubella magna does not seem to be so broadly widespread as the species Endothyranopsis compressus. A considerable contribution of this paper by Vdovenko (1980) is a summary of all

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GLOBAL ZONAL

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TAXA (COMMON FOR ALL PROVINCES)

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ZONE

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Eoparastaffe//a EoefK1othyrai)opsis

Eoparastaffel/a, Eoencbthyranopsis

t--

PROVINCIAL ZONAL TAXA Eurasia

North America

Dainel/a chomatica Eoparastaffella simp/ex Eoendothyranopsis transfta

Eoparastaffel/a ? spiroides Eoendothyranopsis macra

Endothyrp.ex gr. e/egiaPa/aeospiiop/ectammi nadiversa

Endothyra e/egia Encbthyra /arr;e/ata (gr. Encbthyra ex gr. e/egia Pa/aeospirop/ectammina E. e/egia), Tetrataxis diversa Eoendothyranopsis P. mel/ina, Lituotube//a Subgenus Spinoendothyra Encbthyra Global and Encbthyra Global and Encbthyra Spinoendothyra (Spinoendothyra) costifera (Spinoencbthyra) inflata (Spinoencbthyra) E. (S.) paracostifera maxima trachida c tU E. (S) spinosa .!!! Endothyra tU c~ (Latiencbthyra) Encbthyra Subgenus Latiencbthyra Endothyra :s tubercu/ata tubercu/ata (Latiencbthyra) Encbthyra (Latiendothyra) (Latiencbthyra) 0 E. (L.) /atispira/is, E. (L.) Itubercu/ata tubercu/ata subsp. tubercu/ata rjausakensis, E. (L.) crassitheca Genus Chemyshine//a, Chemyshine//a Septabrunsiina Septabrunsiina krainica g/omiformis parakrainica, Chemyshine//a Chemyshine//a tumu/osa Septabru.1Siina kranica Pa/aeospirop/ectammina Chemyshine//a Pa/aeospirop/ectammina tchemyshinensis tumuiosa tchemyshinensis

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E

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Quasiencbthyra kobeitusana Septag/omospiranella primaeva

Subgenus Septag/omospiranella, S. primaeva, Endothyra parakosvensis

Quasiendothyra

Septag/omospirane//a primaeva

Figure 3: Late Devonian-early Carboniferous foraminiferal zonation with typical index taxa. Modified after Lipina (1973).

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STAGE

FORAMINIFERAL ZONES

HORIZONS, SUBHORIZONS Russian Platform

Uralodiscus rotundus

Early Tula

Planodiscus primaevus

Bobrikov

z

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w

(/)

::>

Endothyra ex gr. elegiaPalaeospiroplectammina diversa

z

Radaev

Q)

lIych

~

Pesterkov

Elkhov

~

z

c: \-

Druzhinino

Late Kosvin Early Kosvin

Ci)

D::

e:::> 1;)

Eoparastaffel/a Eo endothyranopsis

Ci

Western slope of the Ural

Spinoendothyra

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~

Tuberendothyra Laxoendothyra

Late Kizel

Late Kizel

Early Kizel

Early Kizel

Figure 4: Foraminiferal zonation of late Tournaisian-early Visean. Modified according to Lipina (1979).

the data concerning the stratigraphic utilisation of Visean foraminifers and the correlation of different foraminiferal zonations. Some shorthcomings of the foraminiferal zonation on the Eastern European Platform are improved in refined zonations in more recent papers by V dovenko et al. (1989), Rukina (1992; non vidi-fide Kulagina & Sinitsyna, 2000), Kulagina and Sinitsyna (2000) and Gibshman and Kulagina (2001).

2.2

Western Europe

The development of the foraminiferal stratigraphy in this region was begun in the 1960s and is connected with the papers by R. Conil, M. Lys and B~ Mamet. In the initial studies, foraminifers are used for characterizing traditional lithostratigraphic units (Conil & Lys, 1964, and many subsequent

I

-17

2.2 Western Europe

STAGES

FORANUNWERALZONES Dainella efremovi-Rectocornuspira regulafis Loeblichia ukrainica Eostaffella proikensis Howchinia exilis-Lituotubella magna

VISEAN

P lanodiscus eospirillinoides Permodiscus rotundus-Propermodiscus Omphalotis chariessa-Endothyranopsis donica Pseudolituotubella tenuissima-Dainella chomatica

TOURN.

Dainella micula-Endospiroplectammina

Figure 5: Latest Tournaisian-Visean foraminiferal zonation by Vdovenko (1973).

papers). In the late Devonian and early Carboniferous, Mamet (1974) defined zones numbered 1 to 16 on the basis of data on the fauna of calcareous foraminifers in Europe, North America and Asia. Mamet's zonation (Mamet & Belford 1968; Mamet 1974) illustrates considerable progress in the stratigraphic utilisation of calcareous foraminifers in Western Europe in the 1970s. A certain disadvantage of this zonation is the fact that its relationship to conodont zonation is not specified. The Famennian and Tournaisian zones seem to be relatively well usable, and the definition of the base of Zone 10 (the first archaediscids) also seems appropriate. Problematic may be the definitions of Zones 12, 13, 14, whose ranges may overlap. The detailed foraminiferal zonation of the Dinant-Namur Synclinorium extended to further regions of Western Europe and a correlation with con-

n 18


Euroasian Euroasian- ~d~. Euroasian affinities Cordilleran 1! 1! affinities affinities ~ ~

Foraminiferal taxa

Cf1

013

QuasiendO/hyra ex gr. bella Quas.communis communis Quas. tegu/aris tegufaris. Quas. sp. subsp. radials Quas. kobeitusana Quas. konensis ChamyshinaJ/a glomiformis Sep/abrunsiina (Sept.) ex gr. rudis Pa/aeospirop/ectammina tchemysh. Endothyra parakosv. c/avaesep/a......... Granulifere//a Seplsbrunsiina (Spinobrunsiina) Tuberendothyra Paraendo/hyra Eb/anaia·························.··········· Tefralsxis Eotextu/aria diversa Lugtonia rroniUs Endospiropfectammina coniU ValvuUnelfa..................................

•

x

•

x x x x x x • x x

•

cr.;

• Charac/aristic apperance

ere

Cf7

3

x

xx

x

2

2xx22x

•.•• •.•. .•. •.•. ••.

2

x x

xx • 2 (x 1 x ..•.• , ..•••.•••..•••.• ... .... (x)

x x x x 2 xx xx xx xx x 2 x 1 2 x x x (x) x 1 • x x x (X) x x x x x

•x

x x x x x x

....... ... ... ... '" ... ............. ..

Eopsraslsffel/a

Daine//a SesieHa Pachysphaer/na pachysphaerica Eoendothyranopsis ........................ LoebUchia fragiUs PseudolituotubeHa Pseudoammodiscidae Biserie/fa Plectogyranopsis ........................... G/oboendothyra O~ha/otis ex gr. minima Archeediscus (G/omodiscus) Ammarchaediscus (RectDdiscus) EoslsffeHa................................... Nodosarchaediscus Latiendothyran. meneri solida Endospiropfectammina syzranica Koskinotextu/aria PojarkoveUa nibaJis ................ Endothyranopsis ex gr. crassus Archaediscus (Archaed.) st. angulatus Nodosarr:haediscus (Neoarchaediscus) Nodosarr:haediscus (Nodaspetodiscus) Vissariotaxis compressa ....... Endothyra spira Neoarchaediscus incerlJJs CribrosfDmum Howchinia bradyana Bradyna rotu/a ............................. . Pseudoendothyra Asteroarchaediscus Climacammina I..JJebHchia paraammonoides WarnanteRa Janischevskina

endenil ~r .ndem.

1Cf5

Cf4

3 3

x 3 • 3 • 3 XX?XX2 2

:cr.:

Eurasian aff. Increasing cosmopolitan characters

x x

•

x x

1 x

x x x

1

• x • x

x x x x x xx x x x x x x x x x x xx (x) 2 x x x x x (x) x x x x x x x x x x x xx (x) x x x 1? x x x x x x x

....... ... ... ... ... ... ............. .. •x

2 2 2 ....... ... ... ... .. .

3

....... ... ... ... .., .......... .. .

••

•x

....... ... ... ... ... ..................................

?

?

? x

x 1

x

x

x x 1 1 x 1 x x x 1

(x) x

x x x 1

• •

xx

x ?

x x x x

• • ....... ... ... ... ... ... .............................. .... •

x Stratigraphical range in the Franco-Belgian Basin.

• ?

x x

xx xx xx xx 1 1 x x • x x 1 x 1 1 1 ? x 1 (X) 1 1 1

••

••1

xx

x

x 2 x 1 x

x

?

x 1

x xx xx 1 x 2 1 1 1 1 x·

Acme in the Franoc>Belgian Basin

Figure .6: Latest Devonian-early Carboniferous foraminiferal zones with typical taxa in Western Europe. Modified after Paproth et al. (1983).

,

I

I

I

2.3 Central Europe

19

n I

odont and other zonations was presented by Conil in the papers by Conil et ale (1976, 1980) and Paproth et ale (1983; see Fig. 6) . The Conil zonation is prima.rily based on data from the Dinant and Namur Synclinorium and, later, also from the British Isles. Its considerable advantage is the fact that it is correlated with conodont and other zonations and that in many profiles calcareous foraminifers were studied together with the conodonts. Foraminiferal zones are also correlated with zonations established on the basis of corals, spores and ammonoids (Paproth et al., 1983). A shortcoming of the zonation is the fact that for the definition of late Tournaisian zones as well as for the definition of the Tournaisian/Visean boundary, the region of the Dinant Nappe was taken, where in the late Tournaisian only much impoverished foraminiferal communities occur. The Tournaisian/Visean boundary is then defined at the level of a conspicuos facies change connected with the occurrence of rich communities of calcareous foraminifers. In the region of the Namur Synclinorium or in some parts of the British Isles, there were favourable facies conditions for the development of communities of calcareous foraminifers in the late Tournaisian, which then leads to difficulties in stratigraphic correlations (Kalvoda 1982, 1983). Since the definition of the base of the Visean on the basis of conodonts is also not without problems (Lane & Ziegler, 1983; von Bitter et al., 1986), interregional correlations of this boundary have been considerably problematic. A certain formal drawback of the Conil zonation is the fact that the zone Cf2 is denoted as the zone of Tournayella, although rich communities of tournayells appear already substantially earlier and even Coni! himself does not include the leading species of this zone into the genus Tournayella. In the stratotype section of Arundian in Wales Kalvoda (Simpson & Kalvoda, 1987) defines the Viseidiscus eospirillinoides-Glomodiscus oblongus- Uralodiscus rotundus Zone with a broad regional distribution and its modifications in different sedimentary environments. Further modifications and improvements of the Coni! zonation were made in subsequent papers by Coni! etal. (1989) and Hance etal. (1994).

2.3

Central Europe

The first authors to deal with the stratigraphic utilisation of calcareous foraminifers in the late Devonian and the early Carboniferous were Dvorak and Conil (1969) who compare the communities found here with those of

I I

!

20


Belgium. In a further paper, Conil (1977) separates the Quasiendothyra communis and Quasiendothyra kobeitusana zones in the Famennian, the Chernyshinella glomiJormis Zone in the Tournaisian and a zone of primitive Archaediscidae in the Visean. Mamet distinguishes some zones of his zonation in Moravia and in Poland (Boucek & Mamet, 1971; Alexandrowicz & Mamet, 1972; Gorecka & Mamet, 1970). In the Visean on the SE slopes of the Bohemian Massif, Kalvoda (1981) distinguishes the Koskinotextularia -Pojarkovella nibelis and Neoarchaediscus zones. Later Kalvoda (1982, 1983) points out that the Belgian zonation of Conil (Conil & Lys, 1964, Conil et al. 1976) can not be applied without important modifications in Moravia and for the late Devonian and the early Carboniferous in Moravia, he defines twelve preliminary foraminiferal zones which he denotes by numerical symbols (Kalvoda, 1983). The regional Moravian foraminiferal zonation, including five zones in the late Devonian and nine zones in the early Carboniferous, was presented by Kalvoda (1989a, 1990).

2.4

Central Asia

Bogush and Yuferev (1962) distinguishes a "zone with Quasiendothyra communis" in the late Famennian of the region Karatau and Talassian Alatau. In the upper Tien Shan Poyarkov (1969) distinguishes the Orientina multicamerata-Tikhinella Jringa-Eogeinitzina devonica Zone in the Frasnian, Parathurammina crassitheca-Neoarchaesphaera polyphora Zone in the early Famennian and the Quasiendothyra communis-Septaglomospiranella grozdilovae-Parathurammina vasiljevae and Quasiendothyra kobeitusanaQuasiendothyra konensis zones in the late Famennian-early Tournaisian. Further relatively detailed foraminiferal zonations, subdividing the late Famennian and early Carboniferous come from Skvortsov (1972), Mikhno and Balakin (1975) and Poyarkov and Skvortsov (1977). Their correlation according to Poyarkov and Skvortsov (1977) is given in Fig. 7. Some zones in Poyarkov and Skvortsov (1977) have a purely local character reflecting unfavourable facies for foraminifers. This primarily concerns zones in the lower part of the Visean, i.e. the Tetrataxis perfida and Omphalotis paraturkestanica zones and in part the Pseudoammodiscus paraprimaevus and Viseidiscus primaevus zones. Although this foraminiferal zonation is quite detailed, the fact that it is not related to the conodont or some other zonations makes correlations with other regions, particularly in the lower

n

--2.4 Central Asia

21

n i

I

,

I i

Unified scheme of Central Asia

-

Mikhno & Balakin 1975

Poyarkov& Skvortsov 1975

Skvortsov 1975

CD

i

Zone

c

Eosfaffella varvariensis

rn

CIS

'i:

Zone

Sediments not studied

CIS CD

.-

II)

Eosfaffe/la protvae

Globivalvulina parva

Eosfaffella oblonga

Eosfaffella oblonga

Archaediscus gigas

Archaediscus gigas

Edofhyranopsis compressa

Endofhyranopsis compressa f'lanoarchaediscus spirUlinoides Ammodiscus (?) ovoides

f'lanoarchaediscus spirillinoides

>

.. c

c

Tetrafaxis kiselica

Endofhyra parafurkesfanica

Endofhyra DBrafurkesfanica

Endofhyra cosfifera

CIS

...::I 0 I-

-

Eoendofhyranopsis aksarsaica Ammobaculiles fchatkalicus

Endofhyra frhikmanica Bisphaera malevkensis

Monofaxinoides transiforius Neoarchaediscus DBrvus Howchinia gibbs longa Neoarchaediscus parvus

Sepfabrunsiina donica

.. . c

'S:

a

..c:: ~

::I

Q.

GI

II)

Forschiella prisca Bradyina rotula

f'lanoarchaediscus spirillinoides

f'lanoarchaediscus spin71inoides

5 f>seudoammodiscus

.

c

GI

III

>

Tefrafaxis pertida

CIS U.

Sepfaglomospiranella

Sepfatournayella lebedevae

f'seudoammodiscus paraprimaevus Visediscus primaevus Tefrafaxis pertida

Omphalofis Omphalofis parafurkesfanica DBrafurkesfanica Dainella chomafica Dainella chomafica Endofhyranopsis - Endofhyranopsis michofi michofi Endofhyra Endofhyra furkesfanica furkesfanica f'lanoendofhyra f'lanoendofhyra c c fchikmanica fchikmanica 'iii 'iii Bisphaera 'ji 'ji c c malevkensis ::I ::I Ear/andia minima

.

.

.. .

~

~

E

..

E

LL

LL

Quasiendofhyra konensis

C CD E

Monofaxinoides fransiforius Neoarchaediscus regularis Howchinia gibba longa Neoarchaediscus parvus

Forschiella prisca Endofhyranopsis crassa

paraprimaevus Visediscus primaevus

Tefrafaxis kiselica

CIS

c

III

GI

Ammodiscus pricus

,II) ,-

Eosfaffella posfmosquensis - E. pseudostruvei III

..

::I

z

Globivalvulina parva

Zone

.!Ii. ..c::

c

CIS

c

.. ..E

';:

::I

E Z

Zone

..

Quasiendofhyra kobeifusana - Q, konensis Quasiendofhyra communisSepfaglomospiranella grozdilovae

Figure 7: Comparison of latest Devonian-early Carboniferous zonations in Central Asia. Modified after Poyarkov and Skvortsov (1975).

22


part of the Visean, difficult. On the other hand, in the late Tournaisian and midle-Iate Visean, when a close connection to the North Paleotethyan Realm is apparent, the Central Asian foraminiferal zones are well correlated. In southern Kazakhstan, Marfenkova (1978) defines four zones in the Visean (see Fig. 8). Vdovenko (1980) differentiates the Visean zones of Tetrataxis eominima-Planoarchaediscus spirillinoides, A rchaediscus moelleri-Parastaffella struvei and Neoarchaediscus incertus-Howchinia gibba in central Kazakhstan. According to Lytvinovich et al. (1981), the following zones are classified in the Famennian of central Kazakhstan: Septaglomospiranella, Quasiendothyra communis, Quasiendothyra communis-Quasiendothyra mirabiliformis, Quasiendothyra kobeitusana -Quasiendothyra konensis. Lytvinovich also defines in the boundary deposits of the Devonian and the Carboniferous, a zone with thin-walled Quasiendothyra kobeitusana.

2.5

Iran and Afghanistan

In the early Carboniferous of Iran Bozorgnia (1973) distinguishes the Earlandiaminor, Septabrusinia krainica, Eotextularia diversa, Dainella chomatica, Uralodiscus rotundus-Paraarchaediscus rigens, Rugosoarchaediscus-Endothyra omphalota parvula-Archaediscus convexus parvula and Neoarchaediscus-Howchinia gibba-Bradyina rotula zones. In Afghanistan, Vachard (1980) defines the C 1 Zone with Earlandia, Tetrataxis and Stacheoides, the C 2 Zc;:me with Eotextularia and Draffania, the C 3 Zone with Viseidiscus explanatus, the C 4 Zone with Viseidiscus eospirillinoides and the C 5 Zone with A rchaediscus krestovnikovi.

2.6

Western Siberia

The zonation of late Devonian and early Carboniferous sediments is similar to zonations valid in eastern Europe and in the Urals. There are, however, little data available from that region, as Paleozoic strata are covered by younger sediments and the data are restricted only to boreholes. The foraminiferal zonation by Bogush (1985) is given in Fig. 9.

2.7

The Central Part of Siberia

In the Verkhoyansk region, Bogush and Yuferev (1966) defined the Endothyra tuberculata and Eoendothyranopsis ermakiensis zones in the early

n

-23

2.7 The Central Part of Siberia

~

bI)

= 00 .....

.

= S= ..... ~ = = IS ~

~,.c= ~

~~

Southern Kazakhstan Zone ChuBetpakdala

......= .=

Zone

e"-

rl..!

~

=

~

Cd

.= .N ."-.-

= ....= ~ ~

>

= = > =

.==.-

.!;C

Propermodiscus krestovnikovi

~

~

rIl

·s ta (f)

Planoarchaediscus spirillinoides

~

....= ....= ~

= •= =

0 ~

=

==e

...c.rI..!

~

Chonetes nalivkini, Verkchotomia plena

......= .= ~

e"-

=

~

~

:s

S

~

~

Omphalotis minimaViseidiscus primaevus

Pseudoammodiscus priscus

.= .."-N.-

Propermo.discus krestovnikovi, Glob oendo thyra globulus spirillinoides

Viseidiscus primaevus

Limestones, calcareous shales and sandstones with Parathurammina suleimanovi, P. tuberculata Bituminous argilites and sandstones with Orthotetes keokuk

Zone

Planoarchaediscus

OJ) ~

Karatau-Talas Zone

Limestones calcareous shales, sandstones with Tetra taxis eominima, Verkchotomia plena

taN :s on § ~

~

Cd

~

~

rIl

(5

~

ta

~

Figure 8: Early Carboniferous foraminiferal zonation of southern Kazakhstan after Marfenkova (1978).

Ii \i ,

i

,I I

I

24


RUSSIAN PLATFORM AND URAL STAGE Subh.

Horizon ProMn

z

~

Steshev

2

:;)

a. g: w

0

Tarus

~ 0

z

:iIn :>

Veney Mikhailov Aleksino

III

c

i

Tula

'" ~

Bobrikov

~ III c

~ .5

....ro Qj Co

~

Endothyra e/egia, Palaeotextularia diversa, Tetrataxis

In

z« g:

:;)

~

Kizel

~

ID

CI)

.s:::

U

u

>-

c

:Q ~

L:

ro

w

Cherepet Upin

~0

::J

Malevka Zavolga

Central-Western Siberian fold bait

Beds with Eostaffella aft. kasakhstanica, Archaediscus karreri, Howchinia [gibba

Beds with Mediocris, Archaediscus krestovnikovi

Endothyranopsis compressa, Propermodiscus krestovnikovi Uralodiscus rotundus, Planodiscus primaevus

Kosvin (Elkhov)

--.l

z

Endothyranopsis crassa, Archaediscus gigas

Radaev

(J)

Ural·Kazakh flexure

Plectostaffela bogdanovkensis EostaffeJlina protvae, Eosigmoillina explicata, Monotaxinoides subpJana Pseudoendothyra globosa, Neoarchaediscus paNUs

Eoparastaffella simplex, Eoendothyranopsis

a;

:!:

Foraminiferal zones

WEST SIBERIAN PLATFORM

Spinoendothyra costifera, Tuberendothyra tuberculata Chemyschinella glomfformis, Ch. disputabilis Bisphaera ma/evkensis, Earfandia minima Quasiendothyra kobeitusana, Eoendothyra communis

Beds with Mediendothyra excalsaformis, Beds with Palaeotextularia diversa, Eoendothyranopsis Endotaxis Tetrataxis, rare Beds with Palaeotextularia Mediendothyra diversa, Latiendothyranopsis cf. I grandis, Tetrataxis Beds with Beds with Palaeospiroplectammina Septabrunsiina tchemyshinensis, krainica Endothyra inflata

Beds with Beds with Quasiendothyra Quasiendothyra kobeitusana kobeitusana

Figure 9: Foraminiferal zonation of West Siberian Platform correlated with the Urals and East European Platform. Modified after Bogush (1985).

--2.7 The Central Part of Siberia

25

Biogeographical Zone Q) C)

Equatorial

cu

+I

Northern high latitudes

(/)

Biozones EostaffelJa protvae Archaediscus commutabilis

c

ttl

EostaffelJa A rch aediscus

Q) (f)

:>

(

---------------------------------_.----------------

Eoendothyranopsis ermakiensis --------.------------------------------------------

Palaeospiroplectammina diversa - Mediocris c

ttl

'en

(l) ...... co

.....J

'rco

'-

::::s

0

I-

>.

Palaeospiroplectammina diversa - Endothyra kosvensis Endothyra tuberculata ChernyshinelJa - Bisphaera

~

co

w

Quasiendothyra kobeitusana - SeptaglomopiranelJa

Figure 10: Early Carboniferous foraminiferal zonation of equatorial and northern latitude belt after Yuferev (1978).

Carboniferous. In a further paper Yuferev (1973) classifies "beds with Quasiendothyra communis-Planoendothyra", "beds with Endothyra tuberculata- Uralinia", "beds with Endothyra similis-Paraendothyra tchikmanica" "beds with Eoendothyranopsis ermakiensis" and "beds with Archaediscus commutabilis" in the early Carboniferous of the Sette-Daban Range and "beds with Endothyra tuberculata- Uralinia", "beds with Eotextularia diversa-Endothyra kosvensis", "beds with Eotextularia diversa-Mediocris" and "beds with Globoendothyra globulus" in the northern Kharaulakh. In the late Famennian and the early Carboniferous of the Sayano-Altaian region Bogush et al. (1978) define the Quasiendothyra kobeitusana-Septaglomospiranella, Tournayella discoidea-Endothyra parakosvensis, Endothyra tuberculata-Planoendothyra, Omphalotis aft'. excelsa-Eotextularia diversa and Eoendothyranopsis ermakiensis zones and in Upper Altai "beds with Planoendothyra rotai", "beds with Plectogyra evoluta" and "beds with Endothyra excelsaformis".

26


WEST SIBERIAN PLATFORM ST.

Malobachatskii

~ 0.. r--

Krekovskii

~

..c:

Suleimanovel/a kolongensis Cribrosphaeroides irregularis

0

Tomchumychskii

..J

Sukhoi

0

? Tubeporina gloriosa - Auroria sphaerica

Suleimanovella paulis Cribrosphaeroides grandiporus

Cribrosphaerodoides aperlus

Figure 11: Correlation of Devonian foraminiferal zones in the West Siberian Platform and the Kuznets Basin, According to Zadorozhnyi (1987).

n I

27


WESTERN URAL System Series Stage Subst. I

c

Q) C

E .~

Ql C

LL

fm

Q)

Ql

.J C Ql C

(J)

~

LL

Complex with foraminifers

Kushelginskii SeptaglomospiraMurzakaevskii nella nana Reit!.

Parathurammina dagmarae SuI. Eonodosaria Askynskii evlanensis Lip. Late Tikhinella Mendymskii multiformis Lip. Nanicella bella Domanikovyi Byk. Polygonella Sargaevskii horrida (Tchuv.) Early Kynovskii frn

+'

Horizon

c

EASTERN URAL Foraminiferal Horizon zone Foraminifers not found

Makarovskii

Koltuban Fm .

Eonodosaria micraMultiseptida corallina

Foraminifers not found

Pashinskii

.~

c 0

> Q)

I

Q) C

~~

0 ~

"0

:Q ~

Late Early

Cheslavskii Chusovskii Afoninskii Biiskii Koivenskii

Vysotinskii Langurskii

B. bykovaeT. corpulenta

Tubeporina gloriosa C Foraminifers not Suleimanovella .~ Vyazovskii found 0) paulis!fill Early Karpinskii SalpingothurammiIrgizlinskii na spinosa kakvensis C Tyutelenskii Toshemskii ~ Ql a. '81 Vizhaiskii Suleimanovella Kulamatskii kolongensis 0 Sherlubaiskii Saumskii Cribrosphaeroides ::i. C .c Ql apertus o() .-> Saraininskii Siyakskii .J Late

Taltiiskii

I

~

1: Ql

w

Figure 12: Correlation of Devonian foraminiferal zones in the Western and Eastern Ural Zadorozhnyi (1987).

-

Ii I

!i 28


9. Spinoendo.

gLd quadr. ~ l:

9:

C/)

lent

1 ...

~b

z ~ z

? Protogn.

?

::J

?

- - - -- -

a

0:: IIn

Quasiendothyra -Complex-

d N ctI

u..

extra.obliq.

a

if

semlc.

N.termin .

... u..ctI

Conod.

Foram.

Foraminifera

Conod.

Figure 13: Correlation of foraminiferal zones in Western Europe with foraminiferal zones in the Omolon Massif. Modified after Simakov etal. (1983).

In the late Famennian to the lowest part of the Visean, Yuferev (1978) reports five zones common for the equatorial region and northern high latitudes; in the remaining part of the Visean he distinguishes different zones for these two basic paleobiogeographic regions (see Fig. 10). Bogush and Yuferev (in Aksenova et al., 1980) specify the definitions of late Famennian and early Carboniferous foraminiferal zones in the central

.

--

r i

I

29


I • • • • •

• +1

"\-

e .,,- ",Hranice na Mor..

-- «/+' lic .\

OSTRAVA

_"

f·""·.e t·" •••• ""'6-1

,+ ...... +. +, .: :. .. ....\

SCALE

o

50km

••1

AUSTRIA

Pre-Devonian basement

Figure 19: Map of discussed localities and boreholes in Moravia. Modified according to Galle et al. (1988). Bra - Brankyj Cho - Chorynej Dra - DraZovicej Di'e - Di'evohosticej Hn - Hnojru'kj Ja - Janovice; Jabl - JablUnkov; Jablv - JablUnkovj Nit - Nitkovice; Ne - NemCiCkYi Po Potstatj Rat - Ratajej Sla - Slavkovj Sva - Svabenicej Uh - Uhi'ice

Stratigraphical range in Moravia: Late Givetian-middle Frasnian. The upper boundary is documented by conodonts which can be attributed both tQ the Late Mesotaxis asymmetrica and to the Ancyrognathus triangularis Zone (Friakova, 1975; Zukalova, 1981). Occurrence in Moravia: Especially the southern part of the Moravian

-3.3 Foraminiferal Zonation

43

Karst (see Fig. 19) between KHiny and Josefov, borehole Branky 1 in the region "North" on eastern slopes of the Bohemian Massif, boreholes LV 8, LV 9 and LH 50 in the Konlce Devonian. Distribution: N anicells of the same age are know mainly in the Urals and East European Platform (Chuvashov, 1965), in Belgium (Mouravieff & Bultynck, 1966), in Germany (Beckmann, 1950), in the Armorican Massif (Vachard, 1994), Boulonais (Vachard, 1988) Afganistan (Vachard, 1980), in North Africa (Vachard & Massa, 1989; Vachard, 1994). Data on systematics of stratigraphically important taxa: Nanicella uralica was described by Chuvashov (1965), the synonymy was presented recently by Vachard (1994), Nanicella ovata was described by Reitlinger (1954) and Nanicella bella by Bykova (1952), further data on synonymy is from Chuvashov (1965). The classification of Nanicella species has been carried out by Poyarkov (1979). 3.3.2

Multiseptida corallina Interval Zone

Definition: The lower boundary of the zone is given by the first occurrence of Multiseptida corallina BYKOVA, the upper boundary then by the occurrence of Eonodosaria evlanensis LIPINA. Characterization: The zone is characterized by the presence of Multiseptida corallina BYKOVA, Tikhinella, Nanicella porrecta BYKOVA and Nanicella tchernyshevae LIPINA, which probably emmerged somewhat later than first Multiseptida and continue together with Multiseptida to the overlying zone. The presence of tikhinells-Tikhinella Jringa BYKOVA and Tikhinella multiJormis (LIPINA)-is recorded in the whole zone and continues in the overlying zone as well. According to its definition the zone represents a lowest-occurrence interval zone. Type locality: Borehole Branky 1, core No. 13 in the region "North" (see Fig. 19). Occurrence in Moravia: Mokra Quarry in the southern part of the Moravian Karst (Hladil et al., 1989), borehole Branky 2, J abliinka 1 in the region "North" (Zukalova, 1983). Distribution: Multiseptida corallina was reported mostly from the Fennosarmatian Province (Kalvoda, 2001). In the Siberian Realm, the morphologically very similar genus JuJerevella ZADOROZHNYI, 1987 occurs in the Kuznets Province and it has been reported also from west-central Alaska (Mamet & Plafker, 1982). It includes two species, JuJerevella tomiensis ZADOROZHNYI and JuJerevella plaJkeri (MAMET) (Zadorozhnyi, 1987; Ma-

n I

44

3 Late Devonian-Early Carboniferous Foraminiferal Zonation in Moravia

met & Plafker, 1982). Toomey et al. (1970), Toomey (1972) and Marchant (1987) reported Multiseptida or Multiseptida corallina from western Canada and Mamet and Plafker (1982) from Alaska and western Canada (British Columbia and Alberta). Recently Multiseptida corallina was reported by Metzger (1989) also from north-central Iowa. Stratigraphical range in Moravia: Middle part of Frasnian-late Frasnian, from the undistiguished Late Mesotaxis asymmetrica-Ancyrognathus triangularis Zone roughly to the base of Palmatolepis gigas Zone. Data on systematics of stratigraphically important taxa: Multiseptida corallina was described by Bykova (1952) and represents the only species of the genus. 3.3.3

Eonodosaria evlanensis Range Zone

Definition: The zone is defined by the first occurrence of Eonodosaria evlanensis. The upper boundary coincides with the extinction of this species and most of the characteristic taxa mentioned below at the Frasnian/Famennian boundary. Characterization: The presence of the species of Eonodosaria, Eogeinitzina, Frondilina and first primitive Tournayellidae is typical. Eonodosaria evlanensis LIPINA, Eonodosaria rauserae LIPINA, Eonodosaria cf. stalinogorski LIPINA, Eogeinitzina devonica LIPINA, Eogeinitzina rara LIPINA and Frondilina sorroris BVKOVA are most characteristic species. Nanicella evoluta REITLINGER seems to be characteristic among nanicells. The presence of tikhinells-Tikhinella fringa BVKOVA and Tikhinella multiformis (LIPINA)-is recorded in the whole zone. The upper boundary coincides with the extinction of all the mentioned taxa except Tournayellidae at the Frasnian/Famennian boundary. According to this definition, the zone represents a range zone of Eonodosaria evlanensis. Type locality: Lesni lorn Quarry, Brno-Lisen (southern part of the Moravian Karst), northwestern part of the upper floor. The boreholes Horakov SV 3 in southern part of the Moravian Karst and JablUnka 1 in the region "North" (see Fig. 19) are counted among other important localities. Stratigraphical range: Palmatolepis gigas Zone. Older data on possible presence of Eonodosaric., and Eogeinitzina in the earliest Famennian of Eastern Europe could not be confirmed. The presence of Multiseptida in the early Famennian of IVforavia (Friakova et al., 1975; Hladil et al., 1989) proved to be erroneous. Th'e early Famennian conodonts of the Palmatolepis crepida Zone were derived from thin neptunian dykes penetrating


45

the limestones. Metzger (1989) reports Eonodosaria evlanensis from Iowa and correlates its occurrence with faunal unit 7 and 8 of Klapper and Lane (1989). Remarks: The Eonodosaria evlanensis Zone was defined first by Zadorozhnyi (1987) in the Frasnian of Western Siberia. Occurrence in Moravia: Southern part of the Moravian Karst (Hladil et al., 1992), regions "South", and "North" on the eastern slopes of the Bohemian Massif. It occurs together with conodonts of the Palmatolepis gigas Zone up to the Palmatolepis linguiformis Subzone (Hladil et al., 1992; Hladil & Kalvoda, 1993). Distribution: Similar assemblages as in Moravia are know especially in the North Paleotethyan Realm-in the Urals (Lipina, 1950; Reitlinger, 1954; Konoplina, 1959), in the Tien Shan (Poyarkov, 1969), in Central Asia (Sabirov, 1980), and in China (Jiaxing & Yichun, 1982). Similar assemblages have also been recorded in the North American Realm (Toomey etal., 1970; Marchant, 1987; Mamet & Plafker, 1982; Metzger, 1989) as well as in the Siberian Realm-in the western part of the Siberian Platform (Zadorozhnyi, 1987) and at the margins of the Kuznets Basin (Menner & Reitlinger, 1971; Zadorozhnyi, 1987). Data on systematics of stratigraphically important taxa: Eonodosaria evlanensis, Eonodosaria rauserae, Eogeinitzina devonica and Eogeinitzina rara were described by Lipina (1950) as well as Nanicella tchernyshevae. Nanicella porrecta, Multiseptida corallina, and Frondilina sororis were described by Bykova (1952). Further data on synonymy and classification were presented by Pbyarkov (1969, 1979), Zadorozhnyi (1987). Vachard (1994) regards Eonodosaria and Eogeinitzina as synonyms. Even though his view is probabbly correct, the traditional systematic approach was still used in this paper. 3.3.4

Eonodosaria evlanensis- Quasiendothyra communis Interzone

Definition: The range of the zone represents an interval between the lower boundary defined by the disappearance of Eonodosaria evlanensis LIPINA and other Eonodosaria, Eogeinitzina, Frondilina, Nanicella (FrasnianFamennian boundary extinction event) and the upper boundary defined by _the entry of Quasiendothyra communis (RAUSER). Characterization: Foraminiferal assemblages of the zone are characterized by the predominance of primitive unilocular foraminifers and by the

n

46


rare presence of primitive Tournayellidae. According to the definition and characterization, the zone represents an interzone.· Type locality: The northwestern part of the upper floor in the Lesnf lorn Quarry, Brno-Lfsen, Horakov SV 3 borehole represents further important locality. Occurrence in Moravia: Abundant in the Moravian Karst and in regions "South", "Centre" and "North" (see Fig. 19). Distribution: The impoverishment of foraminiferal assemblages with preferential survival of euryfClJcial forms can be traced in the early Famennian of all palaeobiogeografical realms and reflects an event of worldwide extent (Kalvoda 1986). 3.3.5

Quasiendothyra communis-Quasiendothyra regularis Interval Zone

Definition: The entry of Quasiendothyra communis (RAUSER) marks the lower boundary, Quasiendothyra regularis LIPINA is typical in the upper part of the zone and the entry of Quasiendothyra kobeitusana (RAUSER) and Quasiendothyra konensis (LEBEDEVA) defines the upper boundary of the zone. Characterization: Quasiendothyra bella (CHERNYSHEVA) and Septatournayella rauserae LIPIN A occur near the lower boundary of the zone in which septabrunsiins-Septabrunsiina nan a (REITLINGER), Septabrunsiina kingirica (REITLINGER), Septabrunsiina primaeva (RAUSER) and Septabrunsiina compressa (LIPINA)-are also abundant. Two subzones can be indentified. The lower subzone is characterized by the presence of Quasiendothyra communis (RAUSER), Quasiendothyra bella (CH~RNYSHEVA), SeptatournayeZZa rauserae LIP INA and forms transitional between septabrunsiins and quasiendothyrs. The presence of Quasiend(i)thyra regularis LIPINA and the radiation of Quasiendothyra exgr. communis (RAUSER) is characteristic of the upper part of the zone, where primitive representatives of Laxoendothyra parakosvensis (LIPINA) occur as well. According to the definition and characterization, the zone represents a lowest-occurrence interval zone. Type locality: Northern wall of upper floor of the Lesni lorn Quarry, Brno-Lfsen, southern part of the Moravian Karst (samples 1-14; Friakova & Kalvoda, 1986). The borehole Horakov SV 1 represents a further important lo"cality. Stratigraphical range: The lower part of the Late Famennian from the

n i

-

-

3.3 Foraminiferal Zonation

47

Palmatolepis marginifera Zone to the Middle Palmatolepis expansa Zone. The upper subzone ranges from the boundary interval of the Palmatolepis postera and Palmatolepis expansa Zone to the upper boundary of the Quasiendothyra communis-Quasiendothyra regularis Zone. Occurrence in Moravia: Abundant in southern part of the Moravian Karst and regions "South", "Centre" and "North" (see Fig. 19). It also occurs rarely in the Konice Devonian. Distribution: Quasiendothyrs of this zone are known mainly in the North Paleotethyan Realm (Kalvoda, 1981). In the Siberian Realm, the fauna of this zone has been recorded in the Omolon and Kolyma massifs and adjacent areas (Bogush & Yuferev, 1970; Simakov etal., 1983). In North America, Quasiendothyra fauna has not been reported at this level. Data on systematics of stratigrafically important taxa: Quasiendothyra bella was described by Chernysheva (1940), Quasiendothyra communis and Quasiendothyra kobeitusana by Rauser (1948), Quasiendothyra regularis by Lipina (1955) and Quasiendothyra konensis by Lebedeva (1956). The systematics of these quasiendothyrs is discussed by Reitlinger (1962). Durkina (1982) has published a more detailed classification of quasiendothyrs, however, the distinction of some taxa is quite difficult and data on their wider distribution are still absent. More data on synonymy of quasiendothyrid species can be found in Bogush et al. (1987). 3.3.6

Quasiendothyra kobeitusana- Quasiendothyra konensis Interval Zone

Definition: The lower boundary of the zone is based on the entry of Quasiendothyra kobeitusana (RAUSER) and Quasiendothyra kon.ensis (LEBEDEVA). The upper boundary is defined by the the occurrence of Tournayellina beata (MALAKHOVA). Characterization: The zone is characterized by a wide areal distribution and considerable variability of quasiendothyrs, Laxoendothyra nigra (CONIL et LYs) and Brunsiina uralica LIP INA being further typical taxa. The representatives of Septabrunsiina, Septatournayella and Laxoendothyra parakosvensis (LIPINA) are abundant as well. According to the definition and characterization, the zone represents a lowest-occurrence interval zone where the lower boundary is defined in the phyletic lineage. Type locality: Lesni lorn Quarry, Brno-Liseii, southern part of the Moravian Karst, eastern wall of the quarry (Kalvoda & Kukal, 1987). The Mokra cement quarry represents a further important locality.

n I ,

II

I

I

I I

I

-

Tl I

48


Stratigraphical range: Latest Famennian, ranging from the Late Palmatolepis expansa to the Middle Siphonodella praesulcata Zone. Remarks: This zone can be distinguished especially in shallow water facies of the outer shelf, its distinctions in the facies of the deeper part of the outer shelf and inner carbonate platform is difficult. The zone was defined first by Reitlinger (1964) in Eastern Europe. In Moravia, Conil (1977) distinguished the Quasiendothyra kobeitusana Zone. Occurrence in Moravia: Abundant in the Moravian Karst, it occurs also in the Hranice Paleozoic and in the region "North" (see Fig. 19). Distribution: The zone is widely distributed in the North Paleotethyan Realm (Lipina, 1973), it has been recorded also in Australia (Mamet & Playford, 1968) and in the Kolyma and Omolon massifs, Verkhoyansk Anticlinal Zone and Eltsov Synclinorium of the Siberian Realm (Yuferev, 1973; Simakov etal., 1983; Bogush etal., 1987). Data on systematics of stratigraphically important taxa: Laxoendothyra nigra was described by Coni! & Lys (1964), Brunsiina uralica by Lipina (in Dain, 1953). Systematics of quasiendothyrs-see previous zone. 3.3.7

Tournayellina beata Interval Zone

Definition: The entry of Tournayellina beata pseudobeata REITLINGER et KULAGINA defines the lower boundary of the Zone, the upper boundary being defined by the first occurrence of Chernyshinella glomiformis LIPINA. Characterization: The zone is characterized by a considerable extent of facies unsuitable for the occurrence of multilocular foraminifers. The decline of quasiendothyrs and facial changes occurred in Moravia at least in two steps. The first was connected with the regression after the Hangenberg Event and the second with an important facies change at the base of the Siphonodella sulcata Zone (Sulcata Event-Kalvoda, 1986a). The base is defined by the entry of Tournayellina beata pseudobeata REITLINGER et KULAGINA, in the higher part Tournayellina beata beata (MALAKHovA) occurs. Tournayellina septata LIPINA, Laxoendothyra parakosvensis (LIPINA), septabrunsiins and primitive chernyshinells (Chernyshinella disputabilis DAIN, Chernyshinella crassitheca LIPINA) are present. The increase of the content of agglutinated grains in the structure of tests of different taxa seems to be significant as well. The quasiendothyrs are still quite abundant after the Hangenberg Event, however, become rare after the Sulcata Event (Kalvoda, 1986a). Palaeospiroplectammina tchernyshinensis LIPINA em merges in the uppermost part of the zone. According to its definition

I.

-----

n

I


49

the zone represents a lowest-occurrence interval zone. Type locality: Lesni lorn Quarry, Brno-Lisen, southern part of the Moravian Karst, eastern wall of the quarry (Kalvoda & Kukal, 1987). Mokra cement Quarry represents a further important locality. Stratigraphical range: Latest Famennian-Early Tournaisian, ranging from the Middle Siphonodella praesulcata Zone to the Siphonodella sandbergi Zone. Reworking cannot be excluded in the S. sandbergi Zone in Moravia (Kalvoda, 1991). The occurrence of quasiendothyrs in the Early Tournaisian has been reported in the Omolon region of northeastern Siberia (Siphonodella sulcata-Siphonodella sandbergi Zone; Simakov et al., 1983), in the Urals (Chermnykh et al., 1988; Nemirovskaya et al., 1993) and in China (Mamet, 1993). According to Hance (1996), the Tournaisian occurrences of quasiendothyrs lack published taxonomic descriptions and illustrations making taxonomic comparisons difficult and the relation to the standard conodont zonations seems to be questionable. I agree with Hance (1996) that the stratigraphical position of all Early Tournaisian occurrences on the territory of the former USSR have to be reexamined, however, quasiendothyrs in Moravia were found in the same sam pIes as early Tournaisian conodonts and have been illustrated (Kalvoda & Kukal, 1987). Remarks: The entry of Tournayellina beata (MALAKHOVA) approximates the Devonian/Carboniferous boundary in terms of foraminiferal stratigraphy not only in the Czech Republic (Kalvoda & Kukal, 1987) but also in Belgium (Conil et al., 1986), in the Urals (Barskov et al., 1984) and in China (Hance, 1996). The zone largely corresponds to the "zone of unilocular foraminifers" or Malev ka Horizon in Eastern Europe and in China (Hance, 1996), which are characterized by an abundant occurrence of unillocular forms and the rare occurrence of multilocular forms. It may partly correspond to the "zone of rare Quasiendothyra" of Rukina (fide Kulagina & Sinitsyna, 2000) in the East European Platform. Occurrence in Moravia: Southern part of the Moravian Karst. Distribution: The zone is distributed in the North Paleotethyan Realmknown from Belgium, Eastern Europe and China. Data on systematics of stratigraphically important taxa: Tournayellina beata pseudobeata was described by Reitlinger and Kulagina (in Kochetkova et al., 1987), Tournayellina beata was described by Malakhova ~1956), Chernyshinella disputabilis by Dain (1953), further synonymy was presented by Lipina (1965) who described also Chernyshinella crassitheca and Tournayellina septata. A further synonymy of Tournayellina beata

50


(MALAKHOVA) was presented by Bogush and Yuferev (in Aksenova et al., 1980). 3.3.8

Chernyshinella glomi/ormis Interval Zone

Definition: The lower boundary is based on the entry of Chernyshinella glomiformis (LIPINA). The upper boundary is defined by the occurrence of Chernyshinella tumulosa LIPINA. Characterization: Beside the index species, other representatives of Chernyshinella-Chernyshinella triangula LIPINA, Chernyshinella disputabilis (DAIN), and Chernyshinella crassitheca LIPINA-occur frequently. The presence of Palaeospiroplectammina tchernyshinensis LIPIN A is typical as well. Abundant are septabrunsiins, among which Septabrunsiina krainica LIP INA seems to be characteristic. According to the definition, the zone represents a lowest-occurrence interval zone. Type locality: Horakov, doc. point 53/88, southern part of the Moravian Karst. Horakov Za 12 is counted among further important localities. Stratigraphical range: Middle Tournaisian, conodont zone Siphonodella crenulata. Remarks: The zone corresponds to the lower part of the Chernyshinella glomiformis Zone defined by Malakhova (1959) in Eastern Europe as well as to the lower part of the Chernyshinella glomiformis Zone distiguished in Moravia by Conil (1977). Occurrence in Moravia: Southern part of the Moravian Karst. Distribution: Mainly North Paleotethyan Realm, rare in North American Realm. In the Siberian Realm occurrences are concentrated in marginal areas, i.e. the Taimyr and the Verkhoyansk Fold Belt (Yuferev, 1973). Data on systematics of stratigrafically important taxa: Chernyshinella glomiformis was described by Lipina (1948), as well as Palaeospiroplectammina tchernyshinensis. Chernyshinella tumulosa was described by Lipina (1956) who presented further data on synonymy and classification of the above mentioned species. More recent data on the systematics of Chernyshinella glomiformis (LIPINA) and Chernyshinella tumulosa LIPINA were presented by Bogush and Yuferev (in Aksenova etal., 1980). 3.3.9

Chernyshinella tumulosa-Spinobrunsiina Interval Zone

Definition: The lower boundary of the zone is defined by the occurrence of Chernyshinella tumulosa LIPINA, the upper boundary by the entry of Paraendothyra.

-,-3.3 Foraminiferal Zonation

51

Characterization: Spinobrunsiina occurs probably little above the lower boundary of the zone. Chernyshinells are abundant in the lower part of the zone while in the upper part, a considerable impoverishment of foraminiferal assemblages can be traced. Chernyshinells become rare and spinobrunsiins and Laxoendothyra parakosvensis parakosvensis (LIPINA) seem to be characteristic. Endothyra (Tuberendothyra) occurs in the upper part of the zone and Endothyra (Tuberendothyra) tuberculata (LIPINA) probably in the uppermost part of the zone. From the definition follows that the zone represents a lowest-occurrence interval zone. Type locality: Hostenice, doc. point Ho 44A, southern part of the Moravian Karst. Horakov, doc. point 37/88 is further important locality. Stratigraphical range: The upper part of the Middle Tournaisian and lowermost part of the Late Tournaisian, Late Siphonodella crenulata-Siphonodella isoticha Zone-early Gnathodus typicus Zone. M estognathus harmalai Zone of shallow water conodont zonation (von Bitter etal., 1986). Remarks: The zone corresponds to the upper part of the Chernyshinella glomiformis Zone both in Eastern Europe (Malakhova, 1959) and in Moravia (Conil, 1977). Occurrence in Moravia: Southern part of the Moravian Karst, region "North" (see Fig. 19). Distribution: A wide distribution in the North Paleotethyan R~alm (Lipina, 1973), rare data from the Siberian (Verkhoyansk Fold Belt) and North American Realm (Yuferev, 1973; Bogush and Yuferev in Aksenova et al.', 1980; Mamet & Skipp, 1970). Data on systematics of stratigraphically important taxa: Endothyra (Tuberendothyra) tuberculata was described by Lipina (1948), further data on systematics of Tuberendothyra presented Lipina (1977). Data on Spinobrunsiina can be found in Conil et al. (1980). 3.3.10

Paraendothyra Interval Zone

Definition: The lower boundary is based on the entry of Paraendothyra, the upper boundary on the entry of Tetrataxis. Characterization: The evolutionary line from paraendothyrs with relatively small basal suplementary deposits, represented by Paraendothyra tchikmanica (MALAKHovA), Paraendothyra ninae GANELINA and Paraendothyra portentosa CONIL, to forms with large supplementary deposits, represented by Paraendothyra nalivkini CHERNYSHEVA, may be traced within the zone. Further important taxa seem to be Rectoparaendothyra, En-

n I

I

52


dothyra (Tuberendothyra) tuberculata (LIP INA) , Latiendothyranopsis latispiralis (LIPINA), Spinobrunsiina, Pseudoammodiscus, Brunsia. The presence of "large tournayells" - Tournayella discoidea DAIN and Eoforschia moelleri (MALAKHovA)-seems to be characteristic as well. In the upper part of the zone, Spinoendothyra and Inflatoendothyra can be abundant and in the uppermost part of the zone, they may be accompanied by the first Dainella. According to the definition and characterization, the zone can be included in the lowest-occurrence interval zones. Type locality: Hostenice, doc. point 51/44/3, southern part of the Moravian Karst. Stratigraphical range: Late Tournaisian, from the Gnathodus typicus Zone to the base of the Scaliognathus anchoralis Zone, lower part of the Mestognathus praebeckmani Zone in the shallow water conodont zonation (von Bitter etal., 1986). Remarks: The subdivision of the zone into subzones would seem to be probable in the future, using the evolution of Paraendothyra. The zone corresponds to the Tournayella Zone of Conil et al. (1976) defined in the Dinant and Namur Synclinorium. The Moravian Zone contains, however, a more diversifieded foraminiferal fauna, enabling a good correlation with Eastern Europe. In the North American Realm the zone corresponds largely to the Zone of tuberculate foraminifers of Brenckle and Groves (1984). Occurrence in Moravia: Southern part of the Moravian Karst, region "North" (see Fig. 19). Distribution: Widespread in the North Paleotethyan Realm (Conil et al., 1988; Kalvoda, 1983; Hance, 1996), present in the Siberian Realm (Bogush & Yuferev, 1966; Simakov etal., 1983; Ivanova & Bogush, 1983). Paraendothyra is absent in the North American Realm, where only Rectoparaendothyra occurs rarely (P. Brenckle, personal communication). In the Siberian Realm, paraendothyrs with small basal deposits are typical and the occurrences recorded are predominately in the Verkhoyansk Fold Belt and in the Omolon (Yuferev, 1973; Conil et al., 1988). In the Omolon Massif Paraendothyra nalivkini CHERNYSHEVA was also reported (Yuferev, 1973). These regions may have been the centers of the origin of paraendothyrs. Other taxa like Endothyra (Tuberendothyra) tuberculata (LIPINA), Spinoendothyra and Inflatoendothyra serve as a good correlation with the North Am~rican Realm (Brenckle & Groves, 1986). Data on systematics of stratigraphically important taxa: Paraendothyra as well as the genus Paraendothyra nalivkini was described by

--3.3 Foraminiferal Zonation

53

Chernysheva (1940), Paraendothyra tchikmanica by Malakhova (1957), Paraendothyra ninae by Ganelina (1966) and Paraendothyra portentosa by Conil (in Simakov et al., 1983). Further data on systematics of Paraendothyra are by Bogush and Yuferev (1966). Latiendothyranopsis latispiralis was described by Lipina (1955), further data on systematics of Latiendothyranopsis as well as Pseudoammodiscus and Brunsia can be found in Conil et al. (1980). Tournayella disco idea was described by Dain (1953) and Eoforschia moelleri by Malakhova (in Dain, 1953), further data on their systematics can be found in Coni! & Lys (1977) and Bogush and Yuferev (in Aksenova et al., 1980). The systematics of Spinoendothyra, Inflatoendothyra and Dainella is discussed by Lipina (1985) and by Rauser-Chernousova et al. (1996). 3.3.11

Tetrataxis-Eotextularia diversa Interval Zone

Definition: The lower boundary is defined by the occurrence of Eotextularia diversa (CHERNYSHEVA), Tetrataxis being a further important taxon emerging at this boundary. The upper boundary is based on the first entry of Eoparastaffella simplex VDOVENKO. Characterization: The zone is characterized by the abundant occurrence of Dainella, especially Dainella chomatica (DAIN), Florennella, in the upper part the gradual increase of Eoparastaffellina, Eoendothyranopsis (Ninella) exgr. donica BRAZHN. et VDOV., Eoendothyranopsis (Ninella) , Pseudolituotubella, Pseudolituotuba, Globoendothyra, Endospiroplectammina, Urbanella appears (see Fig. 20). According to the definition and characterization, the zone can be regarded as a lowest-occurrence interval zone. Type locality: Southern part of the Moravian Karst-Hostenice. Docum. points Hostenice Ho IIB-E. Stratigraphical range: Latest Tournaisian, conodont zone Scaliognathus anchoralis, upper part of the M estognathus prae beckmani Zone in a shallow water conodont zonation (von Bitter et al., 1986). Marchant et al. (1984) report Tetrataxis in the Dollymae bouckaerti Subzone (the upper subzone of the Gnathodus typicus Zone), in Moravia, however, Tetrataxis has so far been found only in the Scaliognathus anchoralis Zone. Remarks: The zone corresponds to the Tetrataxis-Eotextularia diversa Zone of Coni! et al. (1976). In Eastern Europe as well as in Moravia, how_ever, the suitable facies for the expansion of foraminiferal fauna occurred sooner than in the stratotype area of the Dinant Synclinorium and thus the great number of taxa known in the Dinant Synclinorium only during the

54


STAGES

~~

W III

(/) a.

5 ....

Foraminiferal zones Eoparastaffe//a simplex Zone

Tefrataxis Eotextularia diversa Zone

Conodont zones

Eustatic oscillations

Important conodont and foraminiferal taxa

Gnathodus Mestognathus

t~:::s ~::nni Sca/iognathu anchoralis Zone Mast. prae1 - - - - - \ beckmanni Zone

iTrrrrrT " Irrrrrrroillllllill

1111

~ L.!;!;~;!b:....

Q)

.Q

!:l

:S ClJ

& .s..,

••

~

Profile 1

I •

CD

c: 0

N

c co

'iii

~

e 0

....

"§ c: ClJ

~

:S

'mc

::J

.., ;:]

ClJ

} ClJ 0

(J)

Figure 21: Distribution of the genera Eoparastaffella and Eoendothyranopsis in the Tn/V boundary interval in the Mokra quarry near Brno after Ondrackova (2001),


3.3.13

57

Viseidiscus eospirillinoides-Glomodiscus oblongus Interval Zone

Definition: The base of zone is defined by the entry of Archaediscidae represented by Viseidiscus eospirillinoides and other representatives of genera genera Viseidiscus, Planoarchaediscus and a bit higher by Glomodiscus and Uralodiscus. The upper boundary is based on the entry of Pojarkovella nibelis(DuRKINA). Koskinotextularia and Koskinobigenerina enter at a similar stratigraphic level. Characterization: In addition to the above mentioned archaediscid genera, the primitive representatives of Archaediscus ("involutus" type) appear in the zone. The presence of Tournaisian genera Spinobrunsiina, Spinoendothyra, Dainella, Tuberendothyra and Eotextularia seems to be characteristic as well. In the uppermost part of the zone, Palaeotextularia consobrina LIPINA occurs. The definition and characterization suggest that the zone represents a lowest-occurrence interval zone. Stratigraphical range: Early Visean-lower part of the Middle Visean (V1b-V2a of the Belgian division). Type locality: Southern part of the Moravian Karst, Hostenice, profile near the abandoned quarry, doc. points Ho III, IV, Ho Xl, Mokra, doc. point 61, represents further important locality. Remarks: The Glomodiscus oblongus- Uralodiscus rotundus Zone was defined by V dovenko (1980). Kalvoda (in Simpson & Kalvoda, 1987) pointed out the facies substitution between assemblages of the G. oblongus- U. rotundus Zone and Viseidiscus eospirillinoides Zone in the British Isles as well as over the whole North Paleotethyan Realm and defined the Viseidiscus eospirillinoides-Glomodiscus oblongus- Uralodiscus rotundus Zone. An abbreviated form of this zone is used in this paper. Occurrence in Moravia: Southern part of the Moravi;,tn Karst, Nizky Jesenik Mountains, Hranice Paleozoic, region "North" (see Fig. 19). Distribution: Wide distribution in the North Paleotethyan Realm (Vdovenko, 1980; Simpson & Kalvoda, 1987). Impoverished assemblages occur in the North American Realm (Brenckle et al., 1982). The zone cannot be traced in the Siberian Realm. Data on systematics of stratigraphically important taxa: Data on the systematics of Viseidiscus, Planoarchaediscus, Uralodiscus and Glo"modiscus can be found in systematic papers by Pirlet and Conil (1976), Conil et al. (1980), Brenckle et al. (1987) and Vachard (1988a). Viseidiscus eospirillinoides was described by Brazhnikova (in Brazhnikova et al.,

n

58


1967), more data on systematics can be found in Vdovenko etal. (1981). Glomodiscus oblongus was described by Coni! and Lys (1964).

3.3.14

Pojarkovella nibelis Interval Zone

Definition: The lower boundary is based on the entry of Pojarkovella nibelis (DURKINA). Koskinotextularia and Koskinobigenerina represent further important taxa of the zone occurring at the lower boundary. The occurrence of Neoarchaedicus defines the upper boundary. Characterization: The presence of different Pojarkovella, Klubonibelia, Endothyranopsis compressus (RAUSER et REITLINGER), Eostaffella radiata (BRADY) seems to be characteristic of this zone. In the upper part Visarionovella tujmasensis (VISSARIONOVA) and other representatives of the genus appear. Among archaediscids, the representatives of genus Archaediscus ("convexus" type and "concavus" type of Pirlet & Coni!, 1976) and Nodosarchaediscus are significant. In the lower part of the zone, the presence of surviving older taxa such as Spinobrunsiina, Spinoendothyra, Tuberendothyra, Glomodiscus, Uralodiscus and dainellids seems to be typical. The definition and characterization of the zone suggest that it represents a lowest-occurrence interval zone. Type locality: Hosa~nice, the outcrop in the forest north of the village, doc. points Ht 1, Ht 2, southern part of the Moravian Karst. Boreholes Uhrice 14 and Uhrice 9 in the region "South" represent further important localities. Stratigraphical range: Upper part of the Middle and the lower part of the Late Visean. Remarks: '!'he Pojarkovella nibelis-Koskinotextularia Zone was defined first in the Dinant and Namur Synclinorium by Coni! et al. (1976). Pojarkovella nibelis Zone was defined by Altiner (Altiner and Ozgul, 2001) in the Anatolide-Tauride Zone of Turkey. Occurrence in Moravia: regions "South" and "Centre", southern part of the Moravian Karst (see Fig. 19). Distribution: Wide distribution in the North Paleotethyan Realm-East European Platform, the Urals, Central and SW Asia. It is hard to distinguish in the North American Realm and it cannot be distinguished in the Siberian Realm and Perigondwana Realm. Data on systematics of stratigraphically important taxa: Pojarkovella nibelis was described by Durkina (1959), further data on systematics can be found in Simonova and Zub (1975) and Vdovenko et al. (1981). Data


59

on systematics of Archaediscus and Nodosarchaediscus can be found in Pirlet & Conil (1976), Coni! et al. (1980), Vachard (1988a) and on systematics of Koskinobigenerina and Koskinotextularia in Conil et al. (1980). Vissarionovella has been recetly described in a systematic paper by Cosar and Vachard (2001). 3.3.15

Neoarchaediscus Interval Zone

Definition: The lower boundary of the zone is defined by the entry of Neoarchaediscus, the upper boundary by the entry of Loeblichia paraammonodies BRAZHNIKOVA. Characterization: At the· lower boundary, representatives of Archaediscus, referred to as "angulatus" by Conil and Pirlet (1976), occur. Beside the mentioned taxa, the presence of Endothyranopsis crassus (RAUSER et REITLINGER), Bradyina rotula (EICHWALD), Climacammina, Cribrostomum, Howchinia and Monotaxinoides seems to be characteristic. Monotaxinoides and Bradyina rotula (EICHWALD) are typical of the upper part of the zone. According to the definition and characterization, the zone represents an interval zone. Type locality: Marianske udolf near Hranice (Conil, 1977). Boreholes Choryne 9 and Ostravice NP 824 in the region "North" represent further important localities. Stratigraphical range: Middle part of the Late Visean, V3b of the Belgian division, Alexin Horizon and Gnathodus bilineatus conodont zone is reported by Ivanov (1995). Remarks: The zone was first defined by Conil et al. (1976) as the Asperodisc'Us (a younger synonym of Neoarchediscus) Zone. The Moravian zone corresponds, however, only to subzones Q' to {3. Bec-ause of the relatively low surface distribution of limestones representing this zone, a more detailed subdivision (as in the Dinant and Namur Synclinorium) has not been performed in Moravia. Occurrence in Moravia: Boreholes in the regions "North", "Centre" and "South" (see Fig. 19), Hranice Paleozoic. Distribution: The fauna of the zone is widely distributed in the whole North Paleotethyan Realm (Vdovenko, 1980) as well as in the North American Realm (Mamet & Skipp, 1970; Baxter et ai., 1979). The Siberian Realm contains only strongly impoverished foraminiferal fauna which stratigraphical correlation is rather difficult. Data on systematics of stratigraphically important taxa: The data

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proposal presented by Hance and Muchez (1995), who suggested placing the lower boundary of the Visean on the level of the first occurrence of the representatives of the genus EoparastaJJella with a subangular outer periphery (Morphotype 1) which follow the primitive specimens with a rounded periphery (Morphotype 2). This suggestion was made more precise by Hance (1997). On the basis of the ratio elr, where r corresponds to the radius of the largest circle that can be inscribed into the axial section above the umbilici and e corresponds to the height of the axial section above this circle he differentiates two morphotypes of the genus. EoparastaJJella (see Fig. 28). Morphotype 1 is characterized by a well-rounded outer periphery, by the slow to moderate increase in the height of the whorls, the irregular coiling of the inner whorls and a ratio elr ofless than 0.5. As an example, Hance (1997) mentions EoparastaJJella rotunda VDOVENKO and EoparastaJJella ovalis VDOVENKO. Morphotype 2 has a more regular coiling and the ratio elr is greater than or equal to 0.5, which reflects the more rapid increase in the height of

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4 Relation of the Moravian Zonation to Other D-C Zonations

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