GeolCarp_Vol54_No3_139

BRUNOVISTULIAN TERRANE AND ISTANBUL ZONE: TECTONOSTRATIGRAPHIC DEVELOPMENT 139

GEOLOGICA CARPATHICA, 54, 3, BRATISLAVA, JUNE 2003

139152

JIØÍ KALVODA

, JAROMÍR LEICHMANN

, ONDØEJ BÁBEK

and ROSTISLAV MELICHAR

1**

Department of Geology and Paleontology, Kotláøská 2, 61137 Brno, Czech Republic; *dino@sci.muni.cz; leichman@sci.muni.cz;

**melda@sci.muni.cz

Department of Geology, Tø. Svobody 26, CZ-771 46 Olomouc, Czech Republic; babek@prfnw.upol.cz

(Manuscript received April 9, 2002; accepted in revised form December 12, 2002)

Abstract: There are close similarities between the Brunovistulian Terrane and the Istanbul Zone both in the Neoproterozoic

and Paleozoic. The geological structure, lithology and geochronology of the Cadomian Brunovistulicum show broad fit

with the crystalline basement of the Istanbul Zone. Their Gondwana or Baltica affinity is still poorly constrained and

remains a matter of discussion. The Vendian and Cambrian sequences recognized in the central Ma³opolska, Brunovistulian

and Moesian terranes correlate well with the Scythian Platform. In the Istanbul Zone the presence of the pre-Ordovician

sedimentary sequences has not been confirmed and may only be anticipated. In the Paleozoic the best fit was attained in

the DevonianCarboniferous interval. The sedimentary record in the Zonguldak and Istanbul Terranes closely compares

to the Moravian Karst and Ludmírov facies developments of the Brunovistulian Terrane. The correlation is reinforced by

a good fit of the main Variscan deformation phases attributed both in the Brunovistulian Terrane and the Istanbul Zone

to the late Viseanearly Namurian and WestphalianStephanian intervals. This supports, together with the paleobiogeo-

graphic data, the interpretation that the Istanbul and Zonguldak Terranes can be regarded as counterparts of the

Rhenohercynian and Subvariscan Zone in Central Europe. The Istanbul Zone is juxtaposed against the Sakarya Zone

viewed as a part of the Armorican Terrane Assemblage.

Key words: Paleozoic, late Proterozoic, Brunovistulicum, Istanbul Zone, paleogeography, terranes.

Introduction

The Trans-European Suture Zone (TESZ) is a collage of vari-

ous crustal blocks which have been derived either from Balti-

ca or Gondwana and accreted to the Precambrian East Europe-

an Craton (EEC) to form the southern margin of Laurussia

during the Variscan Orogeny. It extends from the North Sea, to

the Black Sea, where the geotectonic position of terranes was

significantly modified still during the Cimmerian events. The

collage includes the £ysogóry, Ma³opolska and Brunovistulian

Terranes in Central Europe, the Moesian Terrane in southeast-

ern Europe and the Istanbul Zone in Asia Minor (Pharaoh 1999;

Belka et al. 2000; Kalvoda 2001). Kalvoda (2001) based both

on similar geotectonic position and paleobiogeographic similar-

ities termed these terranes the Brunovistulian group.

In this paper we review and discuss the evidence for the tec-

tonostratigraphic evolution of the Neoproterozoic basement

and Vendian-Paleozoic sedimentary cover as well as for the

paleobiogeographical record of the Brunovistulian Terrane

and the Istanbul Zone. Some comparison will also be made

with other Laurussian terranes in Central and SE Europe in-

cluding the Ma³opolska and Moesian Terranes and Scythian

Platform (see Fig. 1 and 2) which fringes the southern margin

of the EEC.

Geological setting

In Central Europe the Brunovistulian £ysogóry and Ma³o-

polska Terranes (see Fig. 1) are situated between the Variscan

front and the Trans-European Suture Zone forming the SE

promontory of Laurussia (Kalvoda 2001). It is thought that

both the Brunovistulian Terrane and the Ma³opolska Terrane

were detached from the ancestral Crimea-Dobrogea region

(Scythian Platform) and dextrally transferred along the margin

of the Laurussia during the Variscan time (Lewandowski

1993, 1994; Grygar 1998; Belka et al. 2000). Unrug et al.

(1999) and Nawrocki (2000), on the other hand, stressed the

importance of late Silurian Caledonian movements.

The Brunovistulian Terrane (BVT see Fig. 1) is separat-

ed from the Ma³opolska Terrane by a tectonic unit known as

the Kraków-Lubliniec Fault Zone which is a part of the largely

concealed Hamburg-Kraków Fault Zone (HKFZ see Fig. 1)

parallel to the Trans-European Suture Zone (TESZ).

According to Unrug et al. (1999) the Dobrogean part of the

Moesian Terrane may constitute the prolongation of the

Ma³opolska Terrane to the SE. In the late Triassicearly Jurassic

the Moesian Terrane was sinistrally displaced from the Bruno-

vistulian Terrane along the TESZ during the opening of the pro-

to-Pannonian marginal basin (Banks & Robinson 1997).

According to Pharaoh (1999) the basement of the Moesian

Terrane (see Fig. 2) resembles that of the Ukrainian Shield,

however, the affinity of the terrane is poorly constrained at

present. The Peceneaga-Camena Fault, a NE-vergent Cim-

merian-age thrust juxtaposes Precambrian rocks of the Moe-

sian Platform with Permian-late Jurassic strata of the North

Dobrogea Orogen (Seghedi 1998; Pharaoh 1999).

The Scythian Orogen (Fig. 2) fringes the southern margin of

the East European Craton and was consolidated at the end of

the Late Carboniferous-Early Permian. According to Nikishin

BRUNOVISTULIAN TERRANE (CENTRAL EUROPE) AND ISTANBUL

ZONE (NW TURKEY): LATE PROTEROZOIC AND PALEOZOIC

TECTONOSTRATIGRAPHIC DEVELOPMENT AND PALEOGEOGRAPHY

140 KALVODA, LEICHMANN, BÁBEK and MELICHAR

et al. (1996) this orogenic belt includes the Scythian, Great

Caucasus (Karpinsky Kryazh fold belt), Moesian and Pon-

tides domains and it is viewed as being the eastern prolonga-

tion of the Variscan Orogen of Western and Central Europe.

The Istanbul Zone of the Pontides in northern Turkey was

originally located along the Odessa shelf between the Moe-

sian Platform and Crimea and drifted southward along the ma-

jor transform faults following an oblique slip on the Teissey-

re-Tornquist Zone (TTZ), to form the western Black Sea

Basin during the development of the western Black Sea be-

tween the Albian and early Eocene (Okay et al. 1994; Pharaoh

1999). Close stratigraphic similarities of the Istanbul Zone to

the Paleozoic rocks of the southern margin of Laurasia are

supposed (Görür et al. 1997) and the Cadomian age of the

basement is reported (Kozur & Göncüoglu 1998).

The Istanbul Zone (see Fig. 2) (Okay 1989) of the Pontides

in northern Turkey is separated from the Sakarya Zone by the

Intra-Pontide suture (Okay et al. 1994). Kozur & Göncüoglu

(1998) divided the Istanbul Zone into the Istanbul Terrane

s.str. affected only by Variscan deformation and the Zongul-

dak Terrane which contains mainly Caledonian deformation.

The former is bounded to the west by Strandja Massif, the lat-

ter to the east by Transcaucasia (Kozur & Göncüoglu 1998;

Okay et al. 1994).

Proterozoic basement, Vendian flysch

and Cambrian molasse

Brunovistulian Terrane

Proterozoic basement

The easternmost margin of the Bohemian Massif approxi-

mately between the Danube and the Odra, is built up of a com-

plex of metamorphic and magmatic rocks called the Bruno-

vistulicum (see Fig. 1 BVT) by Dudek (1980), Finger et al.

(2000) or the Brunovistulian Complex (Jelinek & Dudek

1993). The western parts of the BVT were involved in the

Variscan nappe stacking, while the easternmost parts are rela-

tively autochthonous. The eastern, mostly buried part of the

Brunovistulicum, not reactivated during the Variscan oro-

genesis, acted as a stable foreland massif for both, the Variscan

and the Alpine fold belts.

The Brunovistulicum consists of three independent units.

According to Leichmann (1996) the south-western unit or

Thaya Terrane (Finger et al. 2000), ophiolite unit and eastern

unit or Slavkov Terrane can be distinguished from the West to

the East. The south-western complex including the Thaya Plu-

ton, the western part of the Brno Pluton and burried parts

could be interpreted as a large batholith with a complex inter-

nal fabric and evolution including S-, I- and A-type granites.

The geochronological data indicate that the plutonic activity

occurs here in the period between 580 and 590 Ma (Van Bree-

men et al. 1982; Finger et al. 2000; Dallmeyer et al. 1994).

Petrological observation (Leichmann & Hoeck 2002 in prep.),

as well as the high

Sr/

Sr ratio (0.7080.710) and low

Nd 4

to 7 (Finger et al. 2000) indicate that the granites originated

in the volcanic arc environment with important contribution of

older crustal rocks. The widespread dark diorites and tonalites

with lower

Sr/

Sr (0.7050.707) and higher

Nd (1 to 2)

probably represent melts, which brought heat required for ex-

tensive crustal melting. Metasediments were found in the roof

of the granites or only as enclaves. The strong negative

Nd 3

to 7 suggest, that the detritus of these sediments derives from

cratonic crust (Finger et al. 2000).

The ophiolite complex consists of two parts plutonic and

volcanic sequences. The plutonic sequence is metamorphosed

up to the lower amphibolite, and the volcanics into the green-

schist facies (Leichmann 1996). The complex chemistry of the

basalts indicates the supra-subduction zone origin of the ophi-

olites. The observed intrusion relations between granites from

both, south-western and eastern units indicate, that the ophio-

lites are the oldest known part of the Brunovistulicum. The

geochronological data obtained from a rhyolite vein cutting

the metabasalts 725±15 (Finger et al. 2000a) fully confirm

the earlier geological observation. The Slavkov Terrane com-

prises the eastern part of the Brno pluton, Desná Gneiss and

buried parts including Vistulicum and the Upper Silesian

Block. The southern half of this unit consists of primitive

(

Sr/

Sr 0.7040.705

Nd 1 to +3, Finger et al. 2000), I-

type, island-arc granodiorites, tonalites and quartz diorites.

The age determination is less well established in comparison

with the south-western complex. An Ar-Ar hornblende age of

596 Ma was reported by Dallmeyer et al. (1994) only. The

Fig. 1. Structural setting of the Brunovistulian, Ma³opolska and

£ysogóry Terranes. Modified according to Bula et al. (1977).

BVT Brunovistulian Terrane, MT Ma³opolska Terrane,

LT £ysogóry Terrane, HKFZ Hamburg-Krakow Fault Zone,

HCF Holy Cross Fault, TESZ Transeuropean Suture Zone,

MSFZ Moravo-Silesian Fault Zone, PPFZ Peri-Pieninian

Fault Zone, VDF Variscan Deformation Front, CDF Cale-

donian Deformation Front, AF Alpine Front.

BRUNOVISTULIAN TERRANE AND ISTANBUL ZONE: TECTONOSTRATIGRAPHIC DEVELOPMENT 141

granites intrude the metamorphic complex which form the

northern half of the eastern complex.

The metamorphic rocks are known mainly from boreholes.

Variscan overprinted members were reported from the Je-

seníky Mts Desná Gneiss (Finger et al. 2000; Kröner et al.

2000). Most of these rocks are metamorphosed flyschoid

poor greywackes, siltstones and psamites with intracala-

tions of metabasalts and metaandesites (Dudek 1980).

Sr/

and

Nd values (0.7040.706

Nd 1 to +2) are similar to

those of the adjoining granites. Both petrological and isotopic

data indicate in this way a relatively primitive, island-arc

source area of the detritus. The metamorphic grades mainly

reach greenschist to upper amphibolite facies.

Vendian flysch and Cambrian molasse

The crystalline basement of the Brunovistulicum is locally

covered by a Vendian flysch and Cambrian molasse (Fig. 4).

The occurrences of unclear extent are restricted to two areas.

One in the N and NE part of Brunovistulicum which may be

correlated with the Slavkov Terrane and one in the SE part

which corresponds to the Thaya Terrane. Thus, they need not

have been deposited in the same geotectonic position, reflect-

ing the not fully clear course of the Cadomian Orogeny (Fin-

ger et al. 2000).

The sequence of phyllites, metapelites, metapsammites and

metaconglomerates in the N and NE part of the Bruno-

vistulicum is regarded as deposits of a Cadomian foreland ba-

sin (Zelazniewicz et al. 2001).

The Cambrian rocks overlie discordantly the crystalline

and anchimetamorphic rocks (Bula & Jachowicz 1999). The

lower Cambrian siliciclastic sequence dated well by acri-

tarchs occurs mainly in the Upper Silesian part of the terrane

(Bula & Jachowicz 1996), where their thickness increases

markedly towards the east (Bula et al. 1997). Further occur-

rences were detected in the SE part of the Brunovistulian Ter-

rane SE of Brno (Jachowicz & Pøichystal 1997; Fatka & Vavr-

dová 1998).

Fig. 2. Tectonic map of the Black Sea region showing the position of the Moesian Terrane and the Zonguldak Zone. Modified after Okay et al. (1994).

142 KALVODA, LEICHMANN, BÁBEK and MELICHAR

The transgressive cycle of the Gocza³kowice Formation is

formed by a deepening upward sequence of Scolithos sand-

stones, bioturbated sandstones and trilobite siltstones (Bula &

Jachowicz 1996).

Fragments of the middle Cambrian were detected only in

the northern part of the Upper Silesia. Middle Cambrian is

represented by the sequence of alternating layers of quartz and

quartzitic sandstones and laminated sandy siltstone.

In the adjoining Ma³opolska Terrane the oldest rocks com-

prise Vendian folded siltstones and greywackes with interca-

lations of volcanic rocks related to turbidites and debris flows

and resembling those on the adjacent EEC (Moczydlowska

1995; Moryc & Jachowicz 2000). Lower Cambrian conglom-

erates, sandstones, and shales locally overlie discordantly

Vendian rocks.

Istanbul Zone

The basement of the Paleozoic sequence in the Istanbul

Zone is exposed in the Armutlu Peninsula, in the Sunnice

Massif and in the Karadere stream valley (Chen et al. 2002

and references therein). Detailed petrological studies of the

last two areas recently done Ustaömer (1999), Satir et al.

(2000) and Chen et al. (2002).

The basement consits of four units: (1) metasediments, (2)

metagranitoids, (3) metasedimentary-volcanic succesion, and

(4) metaophiolites. The metasediments (1) from Karadere

stream valley contain zircon, which indicates that the clastic

material was derived from 900700 Ma old, probably Afro-

Arabian and E-African crust (Chen et al. 2002). The metasedi-

ments were intruded by calc-alkaline granitoids (2) in the pe-

riod of 590560 Ma. Geochemical data (e.g., low

concentration of high field strength elements), together with

isotopical composition (

Sr/

Sr ~0.705,

Nd 2.12.2) indi-

cate that the granitoids originated in the magmatic arc envi-

ronment. Higher

Sr/

Sr (0.708) and lower

Nd (5) from

some granite indicate possible role of crustal contamination in

the origin of the whole sequence. Geochemical and petrologi-

cal data on granites (Ustaömer 1999), from the Sunnice Mas-

sif are in good agreement with those from the Karadere stream

valley, indicating that the granites in this area represent the

product of an immature arc too.

The field relations, structural characteristic, and geo-

chemical data obtained from the metaophiolites suggest they

were derived in the suprasubduction environment (Yigitbas et

al. 2001).

There are no data on the Vendian flysch and Cambrian mo-

lasse sequences even though some lithologies resemble Cam-

brian sediments of the Brunovistulian or Ma³opolska Terranes.

Scythian Platform and Moesian Terrane

The basement of the Scythian Platform (Fig. 2) comprises

Neoproterozoic granitoid rocks atypical to the East European

Craton (Seghedi 1998; Pharaoh 1999). The Vendian sequence

(Fig. 4) attains 2000 m and contains dominantly coarse ma-

rine deposits which grade upward to continental sequences.

They show some similarities with the Avdarma Group from

the top of the Vendian in the EEC (Seghedi 1998). Lower

Cambrian red-beds are described only in some boreholes.

The affinity of the basement underlying the Moesian Plat-

form (Fig. 2) is poorly constrained at present (Pharaoh 1999).

In south Dobrogea the metamorphic rocks compares to that of

the Ukrainian Shield (Seghedi 1998; Seghedi et al. 2001). In

the northern margin of the platform metabasites and

metapelites of the Altin Tepe Group show a late Proterozoic

metamorphism (696 Ma, K-Ar on biotite) and arc/back-arc af-

finities (Seghedi et al. 2001; Crowley et al. 2000). The low-

grade Neoproterozoic volcano-sedimentary succession over-

lies the basement in South Dobrogea and was deformed at

547 Ma (K-Ar WR) (Kräutner et al. 1989; Seghedi et al. 2001).

In front of the nappes deep water Neoproterozoic-lower Cam-

brian turbidites (Histria Formation) deposited in a foreland ba-

sin were folded and metamorphosed during the Cadomian

events (570 Ma, K-Ar WR) (Kräutner et al.1989; Seghedi

1998).

Ordovician-Permian sedimentary record

In the central European terranes we can distinguish a Ven-

dianSilurian interval during which the terranes are regarded

as independent units and the DevonianPermian interval dur-

ing which the Brunovistulian, Ma³opolska and £ysogóry

blocks were a part of a larger basin at the southern margin of

Laurussia with similar Devonian and Carboniferous lithologi-

cal sequences (Dvoøák et al. 1995; Belka et al. 2000).

Brunovistulian Terrane

Fragments of the Ordovician were detected only in the

northern part of Upper Silesia. Clayey siliceous rocks, light

green interbedded with fine-grained quartz sandstones with

variable degrees of silicification were encountered (Bula &

Jachowicz 1996). Fragmentary record of Silurian sedimentat-

ion is preserved in a tectonic slice in the SW part of the

Brunovistulian Terrane (Kettner & Reme 1936; Chadima &

Melichar 1998), comprising black shales with graptolites and

cephalopods indicating Telychian and Gorstian age.

The rare occurrence of Ordovician and Silurian rocks in the

Brunovistulian Terrane is presumably the result of erosion.

No distinct angular discordance occurs at the Cambrian-De-

vonian contact (Bula et al. 1997).

As already mentioned above, in the DevonianCarboni-

ferous interval the Brunovistulian, Ma³opolska and £ysogóry

Terranes were a part of a larger basin with similar lithological

development. Its key sections are best exposed and studied in

the Brunovistulian Terrane. Devonian to Lower Carboni-

ferous rocks of the Brunovistulian cover provide a complex

record of early Devonian (Pragian) to Tournaisian rifting and

plate extension, Tournaisian to earliest Namurian plate con-

vergence and flysch sedimentation, and Namurian to West-

phalian final plate collision and molasse sedimentation.

Sedimentation in the Devonian to early Carboniferous ex-

tensional regime was associated with a pronounced facies dif-

ferentiation (Chlupáè 1988), a record of which is now pre-

served in the form of three principal facies: the Drahany

(Basinal) Facies, the Ludmírov (Transitional) Facies and the

Moravian Karst (Platform) Facies (Fig. 3). Sometimes the

Vrbno Facies, bearing some similarities with the Drahany

BRUNOVISTULIAN TERRANE AND ISTANBUL ZONE: TECTONOSTRATIGRAPHIC DEVELOPMENT 143

one, is distinguished (Hladil et al. 1999). Lithologic and strati-

graphic data are based mainly on the papers by Zukalová &

Chlupáè (1982), Hladil (1994) and Kalvoda et al. (1999).

The lithostratigraphic succession of the Ludmírov Facies

starts with terrestrial and marine basal clastics of early Devo-

nian age, which are overlain by deep-water, tentaculite- and

trilobite-bearing shales of early Eifelian age. The siliciclastics

pass upward into a succession of upper Eifelian to lower

Givetian carbonates about 250 m thick indicating deposition

in platform margin to platform foreslope setting. In the early

Givetian the carbonate platform margin was destroyed, giving

way to a thinning and fining upward calciturbidite succession

indicating an overall extensional tectonic regime (Bábek

1999). The deposition of carbonates was replaced by pelagic

shales, radiolarites and distal carbonates in early Famennian

Tournaisian, being presumably related to terminal cessation of

carbonate platform growth in the Ludmírov Facies source

area. In the upper part of the sequence intercalations of silici-

clastic turbidites occur.

The oldest rocks in the Moravian Karst Facies are basal

clastics of Emsian to early Frasnian age, comprising terrestrial

and shallow-marine sandstones and conglomerates. The basal

clastics are overlain by a succession several hundreds to about

1000 m thick of Eifelian to upper Frasnian shallow-water car-

bonate platform deposits (see review in Hladil 1986). In the

interval from the early Frasnian to the early Famennian, the

carbonate platform was gradually destroyed due to (present-

day) eastward advance of extensional tectonics, creating a

system of half-graben basins filled with a succession up to

300 m thick of pelagic, red nodular limestones and carbonate

turbidites and debris-flow deposits of early Frasnian to early

Visean age (Kalvoda et al. 1999). In the distal foreland in the

east, carbonate platform sedimentation continued up to the

late Visean. The calciturbidite carbonate successions interfin-

ger and are capped by pelagic, trilobite- and radiolarian-bear-

ing shales in some parts with calciturbidite and siliciclastic in-

tercalations of late Tournaisianmiddle Visean age.

The Drahany Facies, deposited on top of submarine volca-

nic sea-mounts (Galle et al. 1995), bears some similarities

with the Ludmírov Facies (Fig. 3).

The lower Visean to lowermost Namurian siliciclastic fly-

sch, commonly referred to as the Culm facies, is about 7 to

Fig. 3. Schematic correlation of the Paleozoic sedimentation in central and SE Moravia.

144 KALVODA, LEICHMANN, BÁBEK and MELICHAR

12 km thick. The flysch successions in Moravia were consid-

ered by Franke (1995) and Hartley & Otava (2001) to repre-

sent the easternmost continuation of the system of Variscan

peripheral foreland basins filled with deep-water siliciclastics,

which are well known from outcrops and subsurface in the

northern branch of the Variscan Orogen in Western Europe

(Engel & Franke 1983; Leeder 1984). Basic data on the lithos-

tratigraphy, biostratigraphy and general paleogeographical

constraints of the Moravian Culm Basin were given by

Dvoøák (1994), Grygar & Vavro (1994), Kumpera (1983) and

Kumpera & Martinec (1995).

Deep-marine foreland siliciclastics of the Culm facies pass

gradually upward into the Namurian-Westphalian Carboni-

ferous coal-bearing paralic and lacustrine molasse reaching

about 3800 m of thickness. In the eastern part of the Brunovis-

tulian Terrane, molasse deposits directly overlie the pre-flysch

basement.

In the western part of the Brunovistulian Terrane the Permi-

an red siliciclastics of alluvial fan and limnic deposits of the

Boskovice Furrow document the extension connected with

the gravitational collapse of the Variscan Orogen.

Ma³opolska Terrane

In the Ma³opolska Terrane folding, faulting and meta-

morphism to greenschist facies predated the deposition of the

discordant Ordovician-Silurian carbonate/clastic sequence.

Lower Ordovician basal clastics (predominately conglo-

merates) are followed by Ordovician to lower Silurian lime-

stones, Silurian graptolite shales and upper Silurian grey-

wackes with volcanic source rocks (Fig. 4) (Stupnicka 1992;

Unrug et al. 1999). After a period of erosion and faulting,

lower Devonian continental quartzitic sandstones and red

shales were deposited representing the basal clastics, which

start a new deepening upward sequence. They are overlain by

Eifelian to Frasnian carbonates, Famennian shales with lime-

stone intercalations and lower Carboniferous cherty shales

with radiolarites with abundant felsic volcanic detritus. By the

end of the early Carboniferous the deposition of synorogenic

distal flysch started (Dvoøák et al. 1995; Kumpera et al.1995).

The sequence was folded in the late Visean and after a period

of erosion overlain by upper Permian clastics (Stupnicka

1992).

Istanbul Zone

In the Istanbul Terrane sensu stricto the Paleozoic is tecton-

ically superimposed on neighbouring units (Okay et al. 1994).

The data on lithological development are based on papers by

Haas (1968), Görür et al. (1997), Göncüoglu (1997) and Ko-

zur & Göncüoglu (1998).

The oldest sequence of 1000 m of conglomerates, arkosic

sandstones and violet to pinkish mudstones is interpreted as of

alluvial fan origin (see Fig. 4). Its precise age is not known,

but on the basis of its position below overlying lower Silurian

sediments, an Ordovician age is considered likely. Neverthe-

less similar lithologies in the above discussed terranes are also

consistent with a Cambrian age.

The shallow marine sequence starts in the Llandovery with

laminated quartz arenites with Cruziana, interbeds with

greenish grey shale overlain by graptolite shales followed by

lower Silurian shales and siltstones with some limestone beds.

Shallow water limestones were deposited in the WenlockPøí-

dolí interval followed by shallow water limestones and clas-

tics in the Devonian up to the Emsian. Nodular limestones

passing into the overlying fossiliferous shale of Early Devo-

nian age represent a deeper environment. A characteristic

deepening upward sequence (Görür et al. 1997) from middle

Devonian to early Carboniferous starts with alternating calci-

turbidites and shales. Above, with an increasing frequency of

limestone beds, the calciturbidites pass into a typical cherty

and nodular deep-water micritic limestone of late Devonian

age and radiolarian cherts of late Tournaisianearly Visean

age intercalated with shales containing phosphatic nodules.

The presence of turbidites already suggests the transition to

the flysch sequence.

The overlying Culm facies of Thracian flysch comprise al-

ternating greywackes, siltstones and shales. In the upper part

limestone and conglomerate beds with plant remains are also

found. In a few localities the latest turbidites are associated

with shallow marine bioclastic limestones (late Visean) which

are probably olistoliths (Cebeciköy Limestone). Thracian fly-

sch is unconformably overlain by Triassic sandstones.

The pre-flysch sedimentation represents a south facing At-

lantic-type continental margin. The main Variscan event took

place during the early Carboniferous (late Visean to early Na-

murian) (Okay et al. 1994). The Istanbul Terrane is juxta-

posed to the upper plate of the Sakarya Zone (Göncüoglu et

al. 2000) viewed as a part of the Armorican Terrane Assem-

blage (Kalvoda 2002).

In the Zonguldak Terrane (Fig. 4) the data on lithological

development are based on papers by Dean et al. (1997, 2000),

Görür et al. (1997), Göncüoglu (1997) and Kozur & Göncüo-

glu (1998).

Cambrian rocks represented by arkosic sandstones and red-

dish coarse clastics are only anticipated and their Cambrian

age has still not been confirmed (Dean et al. 1997). The Or-

dovician-Silurian sequence starts with sandstones and silt-

stones, overlain by unfosiliferous quartzites. Overlying mud-

stones with a few quartzitic beds of Arenigearly Llanvirn age

are followed by Caradoc black limestones and dark-grey silt-

stones and mudstones. The estimated thickness of the Ordovi-

cian is about 1300 m. In the early Silurian black and grey

graptolitic shales and mudstones with subordinate pelagic

limestone intercalations are described.

The sequence is disconformably overlain by Devonian bas-

al clastics represented by conglomerates, quartzitic sandstones

and shales. The sequence of shallow water platform lime-

stones in the top ranges from Emsian to Visean and is overlain

by middle to upper Carboniferous coal-bearing succession. It

starts with paralic sequence of shales, sandstones and coal

seams of Namurian age followed by Westphalian continental

clastics with the most important coal seams. The contact of

the green-coloured shales and sandstones with red sandstone

intercalations of probably Stephanian age with the underlying

rocks is not clear.

BRUNOVISTULIAN TERRANE AND ISTANBUL ZONE: TECTONOSTRATIGRAPHIC DEVELOPMENT 145

The Caledonian discordance is post-Silurian/pre-Emsian

and is connected with thermal alteration (Kozur & Göncüoglu

1998).

The Moesian Terrane and Scythian Platform

The data on the Paleozoic lithological development in the

Moesian Terrane come from papers by Yanev (1997), Hay-

doutov & Yanev (1997) and Seghedi (1998). The Paleozoic

sequence (Fig. 4) starts with 510 m of Ordovician quartzites

and argillites, nevertheless a Cambrian age in some parts can-

not be excluded. In the Silurian, black and greyish-black

argillites, marls and clayey limestones were deposited. The

lower Devonian pelites are overlain by coarse clastics in the

Middle Devonian. In the top shallow water platform lime-

stones and evaporites were deposited. Biodetrital limestones

dominate over much of the early Carboniferous (Tournaisian

late Visean). The marine environments retreated to the east at

the end of the Visean, and a very thick siliciclastic succession

initially paralic and, from the Namurian to the Westphalian,

limnic, fluvial and coal-bearing was deposited in Dobrogea.

The Permian sediments are typical immature red clastic

rocks, in the upper Permian deposits of anhydrite and halite

also occur.

In the Scythian Platform (Fig. 4) a thick Lower Devonian

terrigenous sequence often unconformably overlies Vendian

deposits, locally Ordovicianmiddle Silurian mudstones, silt-

stones and sandstones occur (Vaida & Seghedi 1997). It is fol-

lowed by a middle-upper Devonian carbonate sequence with

evaporites and thin terrigenous interbeds. The dark coloured

carbonate succession of the early Carboniferous age is over-

lain by paralic and limnic formations of Viseanmiddle Na-

murian age and Permian red clastics (sandstones, aleurites,

argillites), evaporites and volcanoclastic deposits.

The Scythian Paleozoic structures show two important

tectogenetic moments: the late Devonian one which de-

Fig. 4. Correlation scheme of lithological development in the Brunovistulian, Ma³opolska, Moesian, Zonguldak and Istanbul Terranes

and western part of the Scythian Platform.

146 KALVODA, LEICHMANN, BÁBEK and MELICHAR

formed the Vendian-Devonian formations and generated

schistosity and the mid-Carboniferous one of less tectonic

intensity.

Paleobiogeography

CambrianSilurian

In the Upper Silesian part of the Brunovistulian Terrane the

Early Cambrian trilobite associations reported by Orlowski

(1975) are regarded by Belka et al. (2000) as characteristic of

the Baltic Zoogeographic Province. On the other hand

Nawrocki et al. (2001) claimed that the fauna is endemic or

inconclusive for paleogeography. Fatka & Vavrdová (1998)

report a pronounced similarity of the Early Cambrian acritarch

assemblages with the EEC. The Baltic affinity is also inferred

for the Ordovician conodont fauna (Belka et al. 2000).

In the Ma³opolska Terrane Early Cambrian olenellid trilo-

bites are regarded as diagnostic of Baltica (Orlowski 1985;

Belka et al. 2000). In contrast Early Cambrian brachiopods of

Avalonian affinities and different from the EEC are reported

by Jendryka-Fuglewicz (1998). Nevertheless, it should be

stressed that the Ma³opolska Terrane and EEC associations

represent quite different facies-environmental conditions. A

progressive migration of Baltic elements is reported for Mid-

dle Cambrian brachiopod associations and the Ordovician

faunas belong essentially to the Baltic Province (Dzik et al.

1994; Belka et al. 2000).

Obviously the Cambrian paleobiogeographic data show

contradictory results which are often not compatible with the

data on the provenance of clastic micas (Belka et al. 2000).

The Silurian bivalve assemblages from the Moesian Ter-

rane are closely related to those known from the EEC sedi-

ments of Eastern Poland (Iordan 1999). Elements of both

Rhenish and Bohemian faunas are present in the Moesian De-

vonian, as in Poland, Moravia and northwestern Turkey, the

gastropod assemblages being characteristic of the tropical-

subtropical marine conditions of the Old World Realm (Ior-

dan 1999).

In the Zonguldak Terrane Arenig and early Llanvirn grapto-

lites include taxa of both Anglo-Welsh and cosmopolitan af-

finities, Anglo-Welsh late Arenigian trilobites and early Cara-

doc conodonts of the North Atlantic Province (Dean et al.

1997, 2000; Kozur & Göncüoglu 1998). Tremadoc and

Arenig acritarch associations without any Perigondwana cold-

water forms contain cosmopolitan acritarchs and Amorphog-

nathus tvaerensis typical in the warm-water faunas of Scandi-

Fig. 5. Early Carboniferous paleogeographical scheme showing the location of paleobiogeographic units and terranes discussed in the text

with alternative positions of the Sakarya and North Anatolide-Tauride Terranes. According to Kalvoda (2002). Abbreviations: KAZ Ka-

zakh microcontinent, AP Arabian Plate, WC Western Cimmeria, NAT North Anatolide -Tauride Terrane, Sa Sakarya Terrane,

SEU group of South European terranes, I Istanbul Zone, M Moesian Terrane, B Brunovistulian Terrane, Ma Ma³opolska

Terrane, L £ysogóry Terrane, MOLD Moldanubian Terrane, ARM Armorica, EAV Eastern Avalonia, WAV Western Ava-

lonia, IBR Iberia, MEG Meguma, T Turan Terrane, Ta Tarim Terrane.

BRUNOVISTULIAN TERRANE AND ISTANBUL ZONE: TECTONOSTRATIGRAPHIC DEVELOPMENT 147

navia, Estonia and North America. According to Kozur &

Göncüoglu (1998) late Caradoc ostracods and brachiopods of

the Istanbul Terrane include Piretella, a typical Baltoscandian

genus, Klimophores very common in Baltica and also present

in Perigondwana and Eochilina known only in Siberia and

Laurentia. They conclude that the Ordovician had apparently

a warm-temperate fauna with close connection to Baltica and

Siberia/Laurentia but also few connections to Perigondwana.

The interpretation that best fits with available data is that the

Istanbul Zone may have been located close to Baltica already

in the Ordovician.

DevonianCarboniferous

In the DevonianCarboniferous interval, the only data that

could be well applied in all the terranes studied are based on

calcareous foraminiferal fauna. The better application of cal-

careous foraminiferal fauna for paleobiogeographic

interpretations starts with the evolution of multilocular forms

in late Devonian. On the basis of study of late Frasnian, late

Famennian and late Tournaisian-early Visean associations,

Kalvoda (2001) distinguished the Fennosarmatian and Armor-

ican Provinces of the North Paleotethyan Realm (Kalvoda

2002). The Fennosarmatian Province (Fig. 5) also comprised

terranes of the Brunovistulian group which included the

£ysogóry, Ma³opolska, Brunovistulian, Moesian and Zongul-

dak Terrane while the Armorican Province included the Ar-

morican Terrane Assemblage and Intra-Alpine terranes.

The Zonguldak Terrane is a typical part of the Fenno-

sarmatian Province, while the Istanbul Terrane s.str. is includ-

ed because of unsuitable facies for foraminifers with some

reservation (Kalvoda 2001, 2002). The record of foraminiferal

fauna is poor here and richer associations are reported only in

the midle-upper Visean Cebeciköy Limestone (Kaya & Ma-

met 1971; Kaya in Catal et al. 1978) which may represent

olistoliths in the Thracian flysch. The faunal list contains the

typical middle-late Visean North Paleotethyan association of

Eostaffella, Forschiella, Lituotubella magna, Archaediscus

karreri, Vissarionovella tujmasensis, Globoendothyra globu-

lus, Omphalotis omphalota and bilayered paleotextulariids.

Consequently, the Zonguldak and Istanbul Terranes are both re-

garded as a part of Laurussia in similar geotectonic position as

the Rhenohercynian and Subvariscan Zones in Central Europe.

Discussion

Cadomian basement, Vendian-?early Cambrian flysch and

Cambrian molasse

Cadomian basement was found only in the Brunovistulian

Terrane and the Istanbul Zone. Although a perfect fit between

the two units could not be established because of different

size, degree of exploration and different post Variscan evolu-

tion, the broad similarity in the geological structure, lithology

and geochronology between the units point to the possibilty

of their cognate origin (see Table 1).

The broad fit of the geological structure (older ophiolites

and metamorphic rocks surrounded by younger granites) and

of the geochronology between the Brunovistulicum (BVT)

and parts of the Eastern Desert in Egypt (El Gaby et al. 1988)

may indicate a close relation of the BVT to the northern

Gondwana margin during the Panafrican Orogeny (Belka et

al. 2000; Finger et al. 1989; Finger et al. 2000). On the other

hand, there also seems to be a good correlation with the geo-

chronological data from the Urals. On the basis of the Cado-

mian Enganepe 670 Ma ophiolite and 560 Ma calc-alkaline

granites in the Polar Urals as well as on other Cadomian age

intrusives and metamorphites in the central and southern

Urals, Scarrow et al. (2001) hypothesized that the Cadomian

Avalonian arc probably extended along the entire length of

the eastern margin of Baltica. More data on the extent and

geochemistry of the Uralian Cadomides are, however, needed

to establish a more precise correlation with the Brunovistulian

and Istanbul Cadomides.

The limited isotopic data presently available for the Prot-

erozoic basement of the Moesian Terrane do not provide

strong constraints on its affinity. Correlation with the Mora-

vo-Silesian (Brunovistulian) Terrane, which is in a similar

structural position with regard to the EEC, has been proposed

by Burchfiel (1975) and Matte et al. (1990).

The crucial role in the interpretations of the terrane prove-

nance is played by the Vendian and Cambrian sequences. In

central Ma³opolska and the Moesian Terranes and maybe also

in the Brunovistulian Terrane late Neoproterozoic-early Cam-

brian flysch and molasse correlate well with Scythian and

Moldavian Platforms. In the Istanbul Zone Vendian an-

chimetamorphic flysch and Cambrian sediments have not

been detected so far, however, some lithologies may suggest

the presence of Cambrian sediments.

The evidence on the provenance of the terranes is often con-

tradictory, which makes it difficult to formulate a viable tec-

tonic model. Some authors interpret the Brunovistulian

Ma³opolska and £ysogóry Terranes as fragments of Gondwa-

na (Belka et al. 2000) while others prefer origins in E Baltica

Table 1: Schematic comparison of the Neoproterozoic rocks in the

Brno Massif and the Istanbul Zone.

BRUNOVISTULICUM

ISTANBUL ZONE

1) Lithology

Metaophiolites

Metasediments + volcanics

Granites

Metagranitoids, Metaophiolites

Metasedimentary-volcanic succesion

2) Geochronology

Ophiolites < 725±Ma

Granites 580590 Ma

Metasediments ~900700 Ma

Metagranites 560590 Ma

3) Tectonic setting of granitoids 3) Tectonic setting of granitoids

Diorites + tonalites = Volcanic arc

(

Sr/

Sr 0.7050.707; åNd 1 to 2)

Granites = Volcanic arc with crustal

contamination (

Sr/

Sr 0.7080.710;

åNd 4 to 7)

Metatonalites = Volcanic arc

Sr/

~0.705; åNd 2.12.2

Granites = Volcanic arc with crustal

contamination

Sr/

Sr ~0.708; åNd 5

4) Metamorphism

Variablevery low grade to amphibolite

facies. Western part affected by Variscan

tectonics.

Mostly amfibolite facies,strong

deformation, imbrication

148 KALVODA, LEICHMANN, BÁBEK and MELICHAR

(Pharaoh 1999) or in SW Baltica (Zelazniewicz et al. 1997;

Zelazniewicz et al. 2001). In all models there are, however,

some inconsistencies.

In the model of Belka et al. (2000) some detrital micas may

be early Cambrian and thus nearly coeval with the age of the

trilobite fauna of inferred Baltic affinity and the comparison

of micas with the Fennoscandian source in Poland is not com-

patible with significant dextral translation (Lewandowski

1993, 1994; Pharaoh 1999; Winchester et al. 2000).

In the Urals the Cadomian-age orogeny has been well de-

fined up to now only in the Timanides (Scarrow et al. 2001) in

the NE part of the Baltica. It still needs to be better con-

strained and documented outside the Timanides, especially in

the SE and S part of Baltica.

The model of Zelazniewicz et al. (1997, 2001) may be in

contradiction with sedimentological data from the Peri-Torn-

quist and Baltic Basins (Nawrocki et al. 2001; Poprawa et al.

1999).

The paleobiogeographic data in Cambrian are, unfortunate-

ly, not conclusive enough to give an unequivocal constraint to

the paleogeography of the Brunovistulian and other terranes

of the group in Central Europe. Paleomagnetic data suggest

the Early Cambrian nearly equatorial position and its paleolat-

itude differs by about 25° from the coeval paleolatitude of the

closest margin of Baltica (Nawrocki et al. 2001).

In summary it can be stated that the latest Proterozoicearli-

est Paleozoic data are often contradictory and that without a

careful reexamination of biostratigraphic, paleobiogeographic,

geochemic, sedimentological, paleomagnetic and geochro-

nologic data along the TESZ no further advance is possible.

Ordovician-Carboniferous sequences

In the Ordovician most terranes contain arenites with vari-

able amount of shales and argillites. One exception is the

Ma³opolska Terrane, where the basal Ordovician clastics are

overlain by a carbonate sequence, and the second is the Istan-

bul Terrane, where the oldest thick sequence of conglomer-

ates, arkosic sandstones and violet to pinkish mudstones

(Görür et al. 1997) may resemble the Cambrian sequences in

other terranes. In the Brunovistulian Terrane and Scythian

Platform the Ordovician sediments are quite rare.

The Silurian sedimentation is governed by shale facies with

a variable amount of basinal carbonates and rare arenites.

Only in the Istanbul Terrane shallow water limestones pre-

dominate contrary to the Zonguldak Terrane where graptolitic

shales and mudstones with subordinate pelagic limestone in-

tercalations became established. It is quite consistent with

their respective distal and proximal position during the Cale-

donian orogenic event. In our view, the absence of the Devo-

nian unconformity in the Istanbul Terrane may be attributed to

the fact that it represented a distal foreland during the Cale-

donian event. The Caledonian Orogeny is manifested best in

the Ma³opolska Terrane, where a late Silurian flysch sequence

is documented. Again, the Silurian is only rarely represented

in the Brunovistulian Terrane and the Scythian Platform.

The available evidence shows close similarities of all ter-

ranes in the DevonianCarboniferous interval. The basal clas-

tic formation is followed in all terranes by a carbonate prefly-

sch sequence topped either with Culm flysch (proximal fore-

land) and/or coal bearing molasse. In some terranes (Bruno-

vistulian and Istanbul Terranes, partly Ma³opolska Terrane)

deeper sequences represented by calciturbidites, basinal

shales and radiolarites also occur.

There is strong evidence of close similarities both in the

lithological development of the Devonian and Carboniferous

and in the main Variscan events (late Visean to early Namurian

and WestphalianStephanian Okay et al. 1994; Grygar 1997)

between the Brunovistulian Terrane and the Istanbul Zone.

The sediments of the Zonguldak Terrane can be well corre-

lated with the platform Moravian Karst Facies development of

the Brunovistulian Terrane. In the eastern and especially

northeastern part of the terrane, which represented a distal

foreland during the Variscan Orogeny, the same sequences as

in the Zonguldak Terrane were encountered basal clastics,

shallow platform carbonates of the middleupper Devonian

and lower Carboniferous topped by coal bearing Namurian

paralic and Namurian-Westphalian limnic molasse. The same

sequences are also recognized in the Moesian Terrane and in

the Scythian Platform. It may favour the views that assume

the Carboniferous dextral translation of the Brunovistulian

Terrane and locate it in the proximity of the Scythian Platform

(Grygar 1998).

In contrast, the Devonian and Carboniferous of the Istanbul

Terrane correlates well with the Ludmírov facies development

of the Brunovistulian Terrane. In the mentioned areas the

deeper facies of calciturbidites, nodular limestones and shales

topped by shales with radiolarites and Culm flysch are in a

tectonic contact with the basement. We argue that the litho-

logical differences between the Zonguldak and Istanbul Ter-

ranes can be attributed to their distal and proximal position re-

spectively during the Variscan orogenic events.

Consequently, we suppose that the comparison of the Pale-

ozoic sequences of the Istanbul Zone with the southern side of

the Variscan chain (Görür et al. 1997) or with the Intra-Alpine

Terrane (Stampfli 1996; Neubauer & von Raumer 1993; Neu-

bauer 2002) are only very general and based mostly on the

similarities of the Cadomian basement. The Istanbul Zone

represented a lower plate during the Variscan events and a

more plausible alternative, supported both by the paleobio-

geographical and lithological data, is that the zone correlates

very well with the Rhenohercynian and Subvariscan Zones of

the southern margin of Laurussia.

Conclusions

The results of the comparison of the Brunovistulian Terrane

and the Istanbul Zone and their relation to other terranes at the

SE margin of Laurussia can be summarized in the following

points:

1 There is a broad similarity in the geological structure,

lithology and geochronology between the Cadomian crystal-

line units of the Brunovistulian Terrane and the Istanbul Zone

which points to the possibility of their cognate origin.

2 The important role in the interpretations of the terrane

provenance is played by Vendian and Cambrian sequences. In

the central Ma³opolska, Brunovistulian and Moesian Terranes

BRUNOVISTULIAN TERRANE AND ISTANBUL ZONE: TECTONOSTRATIGRAPHIC DEVELOPMENT 149

late Neoproterozoic-early Cambrian flysch and molasse se-

quences correlate well with the Scythian and Moldavian Plat-

forms.

3 The provenance of the Cadomian terranes is still poor-

ly constrained and remains a matter of debate. Besides former-

ly strongly argued views of the Gondwanian origin of all the

Laurussian terranes, a Baltica location of some Cadomian ter-

ranes has recently gained increasing support. To clarify which

alternative is more plausible requires more precise data on the

paleobiogeography, geochronology, geochemistry and loca-

tion of the Cadomian events at the margins of Baltica. Never-

theless, the Ordovician Anglo-Welsh (Perigondwana) fauna

of the Istanbul Zone and the Baltic Ordovician fauna of the

Ma³opolska Terrane raise the possibility of different prove-

nance of Cadomian terranes at the southern margin of Lau-

russia.

4 The sedimentological record of the Istanbul Zone and

the Brunovistulian Terrane in the early Paleozoic (Cambrian

Silurian) is hard to compare because Cambrian deposits in the

Istanbul Zone are only anticipated and the record of Ordovi-

cian-Silurian sedimentation in the Brunovistulian Terrane is

only fragmentary.

5 The good fit of both Ordovician-Silurian and Devo-

nian-Carboniferous sequences of the Zonguldak Terrane and

the Moesian Terrane supports the view that the Istanbul Zone

was located in Paleozoic times along the Odessa shelf be-

tween the Moesian Platform and the Crimea (Okay et al.

1994).

6 There are close similarities in the sedimentary record

of the Brunovistulian, Ma³opolska, £ysogóry and Moesian

Terranes, the Istanbul Zone and the Scythian Platform in the

DevonianCarboniferous interval. The facies and tectonic de-

velopment in the Zonguldak and Istanbul Terrane of the Istan-

bul Zone closely compares with the Moravian Karst and Lud-

mírov development in the Brunovistulian Terrane.

7 Close sedimentological similarities are well in accord

with the late Devonian-Carboniferous paleobiogeographical

data including the Brunovistulian Terrane and the Istanbul

Zone together with the Ma³opolska, £ysogóry, Moesian and

Scythian units in the Fennosarmatian Province, that is to the

southern margin of Laurussia (Fig. 5).

8 The Zonguldak and Istanbul Terranes were in proximal

and distal positions to the orogenic events during the Cale-

donain and Variscan time respectively. In our interpretation

the Istanbul Zone was in similar geotectonic position to the

Brunovistulian Terrane representing the lower plate at the

southern margin of Laurussia during Variscan times. Thus,

the zone cannot be viewed as an equivalent of the Intra-Alpine

or other Variscan terranes of the southern branch. The inter-

pretation that best fits the available evidence is that the Istan-

bul Terrane and the Zonguldak Terrane may thus be correlat-

ed with the Rhenohercynian and Subvariscan Zone of Central

Europe respectively.

9 The Brunovistulian Terrane is juxtaposed to the Mold-

anubian and Saxothuringian terranes representing a part of

Armorican Terrane Assemblage (Kalvoda 2001). Similarly in

Turkey, the lower plate with Cadomian basement and unmeta-

morphosed Paleozoic cover (Istanbul Zone) is juxtaposed to

the upper plate with Variscan granites and high grade meta-

morphites of the Sakarya Zone locally overlain by Carbonifer-

ous-Permian molasse. Even though the age of this juxtaposi-

tion is still a matter of debate the Sakarya Zone can most

probably be regarded as a part of the Armorican Terrane As-

semblage.

Acknowledgments: The study was supported by the research

projects CEZ:J07/98:143100003. We thank professor Demir

Altiner and 2 anonymous referees for valuable comments and

improvements of the text.

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