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Palaeozoic accretion of Gondwana-derived terranes to the
East European Craton: recognition of detached terrane fragments
dispersed after collision with promontories
J. A. WINCHESTER
1
, T. C. PHARAOH
2
, J. VERNIERS
3
, D. IOANE
4
& A. SEGHEDI
5
1
School of Physical and Geographical Sciences, Keele University ST5 5BG, UK
(e-mail j.a.winchester@esci.keele.ac.uk)
2
British Geological Survey, Kingsley Dunham Centre, Keyworth NG12 5GG, UK
3
Ghent University, Palaontologie, Krijgslaan 281/S8, B 9000, Gent, Belgium
4
Faculty of Geology and Geophysics, University of Bucharest, Bucharest, Romania
5
Geological Institute of Romania, 1 Caransebes St, 012271 Bucharest 32, Romania
Abstract: Recent work in Central Europe, combined with emerging information about basement massifs in SE Europe and NW Turkey,
permits a new look at the relationships between crustal blocks abutting the East European Craton (EEC) along the Trans-European
Suture Zone (TESZ). The simplest model indicates that the end-Cambrian establishment of the Bruno-Silesian, Łysogory and
Małopolska terranes close to their present location on the SW margin of the EEC formed a major promontory on this margin of the
continent. Moesia may also have formed part of this block. Both late Ordovician accretion of Avalonia and early Carboniferous accre-
tion of the Armorican Terrane Assemblage (ATA) attached new continental material around the Bruno-Silesian Promontory (BSP).
Palaeozoic faunal affinities and inherited isotopic signatures similar to those of Avalonia seen in the Istanbul block of NW Turkey,
and in minor thrust slices in Moravia and Romania, suggest that easternmost Avalonia was severed, on collision with the BSP, and
migrated east along the southern margin of the EEC. Likewise, the similarities to the ATA of the Balkan, Istranca, Sakarya and
eastern Pontides blocks suggests that more easterly components of the ATA were detached at the BSP and migrated east. All the
newly accreted blocks contain similar Neoproterozoic basement indicating a peri-Gondwanan origin; Palaeozoic plume-influenced
metabasite geochemistry in the Bohemian Massif may explain their progressive separation from Gondwana before their accretion to
the EEC. Inherited ages from Avalonia contain a 1.5 Ga ‘Rondonian’ component arguing for proximity to the Amazonian Craton at
the end of the Neoproterozoic; Armorican terranes lack such a component, suggesting that they have closer affinities with the West
African Craton. Models showing the former locations of these terranes and the larger continents from which they rifted, or later
became attached to, must conform to both these constraints and those provided by palaeomagnetic data. In the late Neoproterozoic
and Palaeozoic, these smaller terranes, some containing Neoproterozoic ophiolitic marginal basin and magmatic arc remnants, probably
fringed the end-Proterozoic supercontinent as part of a ‘Pacific-type’ margin. When this margin fragmented, most resulting fragments
accreted to the EEC.
The SW margin of the East European Craton (EEC) is marked by
the Trans-European Suture Zone (TESZ), traceable from the Black
Sea coast of Romania to North Germany, the Baltic Sea, Denmark
and the North Sea (Fig. 1), despite being everywhere concealed
beneath thick sedimentary cover (Gee & Zeyen 1996; Pharaoh
1999). A description of the nature, age and geometry of this fun-
damental feature of European geology has been provided by
Pharaoh et al. 2006). On the SW side of this zone a collage of
blocks accreted to the EEC margin during the Palaeozoic follow-
ing the end of the Cambrian. SW of the TESZ and north of the
Alpine–Carpathian Front, the basement structure of Central
Europe has long been known in outline. Evidence from geophysi-
cal compilations, geological information provided by deep bore-
holes, and outcrops of Palaeozoic and older rocks across central
Germany and in the Bohemian Massif reveals a mosaic of micro-
continental blocks, derived from different sources and shown by
isotopic dating, and biostratigraphic and palaeomagnetic evidence,
to have become attached to the EEC in their present locations
during the Palaeozoic.
An early phase of terrane emplacement was largely complete by
the end of the Cambrian. These terranes, including the Bruno-
Silesian Terrane, with the Łysogory and Małopolska blocks of
the Holy Cross Mountains in Poland appear to have been situated
in approximately their present position since that time. They may
extend southwards to the Danube, approximately as far as the
Krems–Vienna Line in Austria (Dudek 1980) and also be linked
to the SE beyond the Carpathians with the central and southern
Dobrogea and the Moesian Platform in Romania. Whether these
terranes comprise displaced portions of the EEC (Cocks 2002)
or an early accreted fragment derived from Gondwana (e.g.
Belka et al. 2000, 2002) has been hotly debated, and the arguments
have been set out more fully by Pharaoh et al. (2006). However,
the end-Cambrian attachment of these blocks to the EEC also pre-
cludes any pre-Ordovician association with terranes accreted later,
particularly Avalonia, which was still attached to Gondwana in the
early Ordovician (Winchester et al. 2002). Whatever their deri-
vation, if it is accepted that the subsequent Devonian displacement
of these terranes, suggested from palaeomagnetic and structural
evidence (Lewandowski 1993; Mizerski 1995), was restricted in
extent (Cocks 2002), they must have formed a major promontory
extending from the SW margin of the EEC during most of the
Palaeozoic. This is referred to below as the Bruno-Silesian
Promontory (BSP) and its geometry is crucial in explaining the
mechanisms of attachment of the microcontinents that
subsequently accreted to the EEC.
Excluding the small portions of Laurentian crust forming
Scotland and NW Ireland, the main microcontinental blocks that
subsequently accreted to the SW margin of Europe during the
Palaeozoic are known as Avalonia and the Armorican Terrane
Assemblage (ATA; Franke 2000; Tait et al. 2000). Both of the
latter were derived from Gondwana, but rifted from it at different
times. They therefore possess characteristic Proterozoic basement,
affected by end-Proterozoic Panafrican (locally termed Cadomian)
magmatism and deformation, which therefore does not distinguish
between them.
Factors distinguishing these microcontinental blocks are: (1) the
timing of accretion to the EEC; (2) the presence or absence
of an inherited c. 1.5 Ga ‘Rondonian’ event, which seems, in par-
ticular, also to be a characteristic feature of the ‘Ganderian’
portion of Avalonia; (3) the occurrence of either distinctive
From:GEE,D.G.&STEPHENSON, R. A. (eds) 2006. European Lithosphere Dynamics.
Geological Society, London, Memoirs, 32, 323–332. 0435-4052/06/$15.00 #The Geological Society of London 2006. 323
‘Celtic’ (e.g. Avalonian) faunas that were unique to Avalonia
during the mid- and late Ordovician, or of distinctive mixed
Siluro-Devonian faunas characteristic of the ATA; (4) the pre-
sence of late Ordovician glaciogenic sediments, a Gondwana
feature shared by the ATA, but not by Avalonia, which had by
that time already migrated into lower latitudes (Cocks et al. 1997).
Avalonia
Precambrian and early Palaeozoic basement exposed in central
England, Belgium and western Germany is widely accepted as
part of Avalonia, this Ordovician microcontinent extending west
as far as New England, and being best exposed in the Avalon
Peninsula of Newfoundland, after which it is named.
Avalonian basement in central England typically consists of late
Proterozoic intrusive, volcanic and sedimentary rocks (e.g. Thorpe
et al. 1984; Pharaoh & Gibbons 1994; Strachan et al. 1996),
affected by end-Proterozoic or pre-Early Cambrian deformation.
In the English Midlands it was little affected by later movements,
and is overlain by a thin Lower Palaeozoic shallow marine
sedimentary sequence, succeeded conformably by Devonian ter-
restrial deposits: the ‘Old Red Sandstone’. For this reason it has
sometimes been called the ‘Midlands Microcraton’ (e.g. Turner
1949; Pharaoh et al. 1987). A fuller description has been given
by Pharaoh et al. (2006).
The Midlands Microcraton is flanked to the NW by much
thicker Lower Palaeozoic successions, strongly deformed in an
early Devonian ‘Acadian’ event (Soper et al. 1987), deposited
on Avalonian basement and exposed in Wales, the English
Lake District and SE Ireland. Boreholes in eastern England
reveal that similarly deformed rocks (Pharaoh et al. 1987) con-
taining Upper Ordovician calc-alkaline volcanic rocks, as an
apparent continuation of the Lake District Arc, also extend
from eastern England to Belgium, where they are exposed in
the Brabant Massif (Andre
´et al. 1986; Pharaoh et al. 1991).
These rocks have been termed (Winchester et al. 2002) the
Anglo-Brabant Deformation Belt (ABDB), in which the defor-
mation is inferred to have developed in the early Devonian
(Acadian). This deformation belt is thought to mark a zone of
crustal suturing inherited from the late Ordovician soft collision
of Avalonia and Baltica (Verniers et al. 2002). Unusually thick
lower Cambrian deposits in Brabant suggest the presence of
rifting, which may have thinned and weakened the Proterozoic
basement, thereby controlling the location of this deformation
belt (Winchester et al. 2002). Because the ABDB contains no
known ophiolitic material, it is not thought to mark a zone of
microcontinent collision and seaway destruction, even though,
Fig. 1. A map showing the distribution of crustal blocks and Palaeozoic deformation belts in Central and SE Europe. ABDB, Anglo-Brabant Deformation Belt;
AD, Ardennes; ADF, Alpine Deformation Front; AM, Armorican Massif; BB, Brabant Massif; BK, Balkan Terrane; BM, Bohemian Massif; BSM, Bruno-Silesian
Massif; CACC, Central Anatolian Crystalline Complex; CAU, Caucasus; CD, Central Dobrogea; CDF, Caledonian Deformation Front; CDO, Central Dobrogea;
CM, Cornubian Massif; COF, Capidava–Ovidiu Fault; DR, Dronsendorf Unit; EA, Ebbe Anticline; EL, Elbe Lineament; EP, Eastern Pontides; GF, Gfo
¨hl Unit;
HCM, Holy Cross Mountains; HPDB, Heligoland–Pomerania Deformation Belt; IB, Istanbul Block; IMF, Intra-Moesian Fault; Istr, Istranca Terrane; KLZ,
Krakow– Lubliniec Zone; LU, Łysogory Unit; L-W, Leszno – Wolsztyn High; MC, Midlands Microcraton; MM, Małopolska Massif; MN, Mu
¨nchberg Nappe;
MNSH, Mid-North Sea High; MP, Moesian Platform; MST, Moravo-Silesian Terrane; NASZ, North Armorican Shear Zone; NBT, North Brittany Terrane; NDO,
North Dobrogea; NGB, North German Basin; PCF, Peceneaga–Camena Fault; Pom, Pomerania; POT, Polish Trough; R, Ru
¨gen Island; RFH, Rynkøbing–Fyn
High; RG, Rønne Graben; Rh, Rhodope; SASZ, South Armorican Shear Zone; SBT, South Brittany Terrane; SDO, South Dobrogea; SGF, Sfantu Gheorghe Fault;
SNSLT, South North Sea–Luneberg Terrane; SP, Scythian Platform; S-TZ, Sorgenfrei–Tornquist Zone; Su, Sudetes; TB, Tepla
´–Barrandia; T-TZ, Teisseyre–
Tornquist Line; VF, Variscan Front; ZZ, Zonguldak Zone.
J. A. WINCHESTER ET AL.324
as suggested by Pharaoh et al. (1993), it may separate crusts with
somewhat differing structures.
An area of stable basement, indicated by seismic traverses and
termed the Southern North Sea–Luneberg Terrane (SNSLT) by
Pharaoh et al. (1995), lies east of the ABDB, NE of the Dowsing–
South Hewett Fault Zone– Lower Rhine Lineament, themselves
younger reactivations of earlier major fault-lines (Pharaoh 1999).
It has been more recently dubbed ‘Far Eastern Avalonia’ (Winche-
ster et al. 2002), because of its geological similarities to Avalonia.
Although crystalline basement is mostly concealed, one outcrop
area, the 574 +3 Ma Wartenstein Gneiss (Molzahn et al. 1998),
is exposed far to the south in the South Hunsru
¨ck at the SE margin
of the Rhenish Massif; lying to the south of the Variscan Front,
this typically calc-alkaline granitoid gneiss of late Neoproterozoic
age is broadly comparable with granitoid rocks in the Avalonian
basement in central England. In addition, Samuelsson et al.
(2002a) noted that the 1Nd(t)trendsofOrdoviciansedimentary
rocks from the Ebbe Anticline of NW Germany (Fig. 1), situated
NE of the Lower Rhine Lineament and therefore on SNSLT base-
ment, match those from the Welsh Basin and the Brabant Massif,
but are different from those in Brittany and Iberia. They also
concluded that these rocks formed part of Avalonia.
Hence the ABDB is interpreted as an intra-Avalonian zone of
local subduction, initiated above a failed Cambrian rift, where
the basement had been thinned and weakened, in response to the
distortion and anticlockwise rotation of part of Avalonia as it
moulded itself on to the margins of the EEC and Laurentia (Ver-
niers et al. 2002). The late Ordovician timing of the accretion of
the SNSLT to the EEC (Vecoli & Samuelsson 2001; Samuelsson
et al. 2000b), which only slightly predates Avalonian convergence
with Laurentia, based on evidence from Atlantic Canada (e.g.
Cawood et al. 1994), and the onset of Windermere Supergroup
sedimentation in the English Lake District (Cooper et al. 1993),
also suggests that the SNSLT should be considered as part of
Avalonia. If so, the Heligoland– Pomerania Deformation Belt
(HPDB), which largely comprises a zone of overthrusting,
marks the collision zone between Avalonia and the EEC. It
shows little evidence of contemporary magmatism in boreholes,
but geophysical evidence may indicate the presence of buried
arc volcanic rocks (Williamson et al. 2002; Pharaoh et al.
2006), suggesting that convergence was accompanied by south-
directed subduction beneath the Avalonian margin.
Avalonian easternmost extremities
Although totally concealed by thick Mesozoic and Cenozoic
sequences in the Polish Trough, the easternmost end of Avalonia
appears to abut the Łysogory and Małopolska blocks of the Holy
Cross Mountains, which form part of the Bruno-Silesian Promon-
tory (BSP). Further south, tectonic structures along the western
margin of the Bruno-Silesian Block show highly oblique (dextrally
transpressive), complex overthrusting to the east (Moldanubian and
Drinova thrusts) in the early Carboniferous, between 350 and 330
Ma (Schulmann & Gayer 2000). This junction is traceable north-
wards beneath the thick sedimentary cover of the Polish Trough,
using seismic profiling. Both the Polonaise P1 and Teisseyre–
Tornquist Zone (TTZ) profiles (Grad et al. 1999; Jensen et al.
1999) show a clear change of mid-crustalstructure northof the Mol-
danubian Thrust, suggesting that it continues northward as a major
feature (Moravian Line of Winchester et al. 2002). The TTZ
profile shows the mid-crustal break to be displaced eastwards com-
pared with Polonaise P1, indicating dextral displacement of the Mor-
avian Line by strike-slip faulting between the two profiles, perhaps
along the Dolsk Line (Grad et al. 2002).
On accretion, Avalonia was unlikely to fit exactly into the pos-
ition against the EEC margin that it now occupies, bounded to the
east by the BSP. Therefore, former eastern extensions are likely to
have been detached by shearing initiated by collision with the BSP
(Fig. 2). Recognizing the Avalonian affinities of such detached
extensions, where later metamorphism may have destroyed
faunal evidence, is problematic; discrimination between Avalonia
and the ATA must rely instead on the presence (as in Avalonia), or
absence (as in the ATA) of mid-Proterozoic (1.45 Ga) inherited
zircon dates, related to the previously adjacent (pre-rifting from
Gondwana) Rondonian event in the Amazonian Craton.
Fig. 2. (a) Sketch map illustrating the supposed configuration of Avalonia on
its initial impact with the Bruno-Silesian Promontory. (Note the detachment
and displacement eastward of its eastern extremity). Abbreviations as in
Figure 1. (b) Sketch illustrating the likely configuration of the Armorican
Terrane Assemblage on initial impact with the Bruno-Silesian Promontory in
the early Carboniferous. GWSO, Giessen–Werra– Sudharz Ocean; MGCH,
Mid-German Crystalline High. Other abbreviations as in Figure 1. (c) Likely
configuration of crustal blocks following the main Variscan Orogeny.
(Note the eastward displacement of the eastern Variscides.)
DETACHED TERRANE FRAGMENTS IN EEC 325
The Moravicum Nappe
In NE Austria and Moravia, the Dobra Gneiss (Gebauer & Friedl
1993) and Bittesch Gneiss (Friedl et al. 2000) both yield mid-
Proterozoic inherited zircon dates of c. 1.5 Ga, contemporary with
the Rondonian orogeny affecting the NW side of the Amazonian
Craton (Tassinari et al. 2000; Cawood et al. 2003). They also show
clusters of inherited dates at 1.2 and 1.78 Ga, which have also been
noted both from Ganderian (Avalonian) basement in southern New
Brunswick and from the Amazonian Craton (where they are termed
the Sunsas and Rio Negro provinces; Tassinari et al. 2000).
Because these rocks were thought to be linked to the Bruno-Silesian
massif(BSM),thesedateswereinterpretedtoassignanAvalonian
affinity to the BSM (Finger et al. 2000). However, if the latter was
attached to the EEC, at least since the end of the Cambrian, it
cannot also have been part of Avalonia. However, both the Dobra
and Bittesch gneisses are situated in the deformed Moravicum
nappe, emplaced onto the western margin of the Bruno-Silesian
block by movement on the Drinova Thrust (Hock et al. 1997;
Melichar & Kotkova 2003). They therefore need not belong to the
BSM, and could instead represent small detached slivers of
Avalonian crust thrust obliquely onto the margins of the BSM.
The Danubian basement of the southern Carpathians
in Romania
Exposed in nappes towards the western end of the southern
Carpathians of Romania are rocks of the Lower and Upper
Danubian basements (Berza et al. 1983, 1994, 2004; Iancu &
Berza 2004). Late Neoproterozoic magmatic rocks (Liegeois
et al. 1996) including calc-alkaline granitoids such as the
Tismana Pluton (567 +3 Ma, U – Pb) are unconformably overlain
by a clastic sedimentary succession of Late Ordovician – Early
Silurian age, apparently devoid of recorded glaciogenic diamic-
tites. These rocks underwent a Devonian (?Acadian) deformation
and, although clear faunal or palaeomagnetic evidence remains
lacking, and some claim that the older rocks may be exhumed
Moesian basement (Sandulescu 1984, 1994), these characteristics
make an Avalonian affinity an alternative possibility.
The Istanbul Block
Further east, in the Istanbul Block of NW Turkey, lithologically
similar Ordovician rocks have yielded ‘Celtic’ (e.g. Avalonian)
faunas (Kozur & Go
¨ncu
¨og
˘lu 1998; Dean et al. 2000). Some
studies have distinguished, in this area, separate Istanbul and
Zonguldak terranes, based on differences of facies between
Palaeozoic rocks close to Istanbul and those further east
(Goncuoglu & Kozur 1998, 1999; Kozur & Gincuoglu 2000).
Also, whereas sedimentation near Istanbul seems to have
continued uninterruptedly from the Early Ordovician to the Mid-
Carboniferous, further east there are increased signs of Early
Devonian uplift and deformation. However, no clear boundary
between these terranes can be mapped, and it seems more likely
that these differences relate to facies changes within a single
terrane, analogous to those seen within Eastern Avalonia, in
which Central English and Welsh successions can be contrasted.
According to this analogy, the continuous sequence in the Istanbul
area corresponds better to the Lower Palaeozoic shelf deposits in
Central England, whereas the overlying Upper Palaeozoic rocks,
containing mixed shales, cherts and limestones and their benthic
fauna (Tokay 1955) have more in common with the marine Devo-
nian and Carboniferous units of the Rheno-Hercynian zone, which
in both SW England and Germany overlie Avalonian basement.
By contrast, the Zonguldak area, after the deposition of an
initial pebbly quartzite, reveals a shale-dominated Ordovician
sequence more characteristic of the Welsh Basin, and this
analogy is enhanced by the presence of a Lower Devonian uncon-
formity. Ensuing Late Devonian and Early Carboniferous sedi-
mentation is dominated by limestone, which is in turn succeeded
by regressive flood plain deposits containing coals (Yanev et al.
2006). Both this Upper Palaeozoic sequence and the major uncon-
formity above which Permo-Triassic continental clastic rocks
occur are analogous to the sequence seen in England overlying
Avalonian basement.
The Avalonian link for the Istanbul Block, suggested by both the
lithological sequences and the faunal evidence, is further strength-
ened by a mid-Proterozoic discordia date of 1445 +24 Ma
obtained from a late Neoproterozoic granite in the Karadere base-
ment (Chen et al. 2002). A further, less well-constrained inherited
age of 1189 +110 Ma from a metatonalite in the same area (Chen
et al. 2002) also resembles some of the ages obtained from the
Moravian Nappe, and from the Ganderian part of Avalonia in
southern New Brunswick. This information, combined with evi-
dence of Silurian deformation in the northern part of the block
near Zonguldak (although not nearer to Istanbul itself) also is con-
sistent with Siluro-Devonian docking with Baltica of an Avalonian
fragment, and post-Carboniferous (Variscan) deformation, as in
the Rheno-Hercynian zone of Western Europe, may attest to the
deformation of the southern Avalonian margin caused by accretion
of terranes of the ATA.
Moesia and Dobrogea
In contrast, there is little evidence to link the basement rocks of
any part of either the Moesian Platform or the Dobrogea with
Avalonia. Neoproterozoic and Lower Palaeozoic rocks of the
central and southern Dobrogea, in eastern Romania, appear to
have similarities to those in the Holy Cross Mountains of Poland
rather than the Istanbul Block, and borehole sections indicate
that this is also true of the northeastern part of the Moesian Plat-
form, NE of the Intra-Moesian Fault (IMF). Metamorphic base-
ment to the southern Dobrogea has also yielded Mid-Proterozoic
ages (Giusca et al. 1967), and is considered to have affinities
with rocks in the Ukrainian Massif of the EEC. Residual gravity
and magnetic anomalies also indicate a link with the EEC
(Ioane & Atanasiu 2000). However, as the Bruno-Silesian
Massif itself may also have originated adjacent to the southern
EEC, it is possible that this basement may also underlie the
Central Dobrogea at greater depth. West of the IMF, Neoprotero-
zoic granitoids have also been recovered from boreholes (Savu &
Paraschiv 1985), and Cambrian rocks from deep boreholes (Mutiu
1991) have yielded numerous fragmentary specimens of the trilo-
bites Paradoxides (species undetermined) and Peronopsis fallax
(Linnarsson). A. Rushton (pers. comm.) considered that the latter
fossil, although apparently showing some affinities with species
associated with the Baltican margin (Rushton & McKerrow
2000), is a widely recorded member of an outer shelf fauna,
which may have been able to cross geotectonic boundaries. Thus,
although neither trilobite can be used to prove conclusively a peri-
Baltican affinity of the Moesian Platform, similar to that proposed
for the Dobrogea or Bruno-Silesian regions, this remains its most
likely affinity. However, the presence of a widespread unconfor-
mity beneath Silurian rocks (Iordan 1984) may indicate a Late
Ordovician uplift, which could record deformation associated
with collision of Avalonian fragments immediately to the south.
Avalonian eastern extremities: mechanism
of emplacement
Lower Palaeozoic rocks deposited directly on the EEC margin are
all consistent with a passive margin setting: the narrowing of the
Tornquist Sea appears to have occurred exclusively by subduction
under the Avalonian margin up to the time of collision in the late
J. A. WINCHESTER ET AL.326
Ordovician. Further east, however, the southern margin of the BSP
is now concealed beneath younger rocks associated with the much
later formation of the Carpathians. Yet, for fragments of Avalonia
to migrate east with dextral transpression, continued subduction
was probably needed, but the Silurian rocks in the Istanbul
Block do not include magmatic rocks indicative of continued sub-
duction. It therefore seems likely that, on collision of easternmost
Avalonia with the BSP, a change of polarity of subduction
occurred analogous to that recorded in New Brunswick with
closure of the Iapetus Ocean in that sector (van Staal et al.
1991). With continued subduction, but this time northward-
directed, the buoyant continental fragments of Avalonia could
be transported eastwards with sinistral transpression, along the
southern margin of the EEC, until ‘trapped’ in re-entrants of the
continental margin (Fig. 2a). Smaller fragments, such as the Mora-
vicum Nappe and the Danubian Terrane, may be interpreted as
slivers on the continental margin, abandoned during the eastward
progress of the Istanbul Block.
The present position of the Istanbul Block partly arises from its
southward displacement during the opening of the Black Sea
basins, since the Cretaceous. There seems to be no clear westward
continuation into Moesia or the Dobrogea, which suggests that
almost the entire Avalonian fragment was displaced southwards
as the Istanbul Block.
Accretion history of the Armorican Terrane Assemblage:
mechanisms of migration and ocean closure
The Armorican Terrane Assemblage (sensu Franke 2000; Tait et al.
2000), also previously referred to as ‘Peri-Gondwanan Terranes’ or
‘Northern Gondwana terranes’ (e.g. Erdtmann & Kraft 1999), is
exposed in a series of massifs across much of SW to Central
Europe from Iberia to Poland. In Western and Central Europe,
these terranes were accreted to Laurussia duringthe Late Palaeozoic.
The term ‘Variscan Orogeny’, which has been used to describe the
deformation and magmatism associated with the closure of the
Rheic Ocean, its successor basins, and basins separating constituent
terranes within the ATA, does not fully convey the complexity of
these multiple accretions: a revised overview following intensive
study of the constituent terranes in Central Europe and their
accretion histories has been given by Pharaoh et al. (2006).
In summary, early Devonian metamorphism and magmatism
(sometimes called ‘Caledonian’, but historically and collectively
termed Eo-Variscan elsewhere in Hercynian Europe; e.g. Faure
et al. 1997; Shelley & Bossie
`re 2000) was confined in the northern
Bohemian Massif to isolated high-grade metamorphic rocks in the
Go
´ry Sowie Block (GSB; Brueckner et al. 1996; O’Brien et al.
1997) and the Mu
¨nchberg klippe (395– 390 Ma; Kreuzer et al.
1989; Stosch & Lugmair 1990). It may record local tectono-
thermal and hence collisional activity between migrating platelets
of the ATA, with subsequent exhumation. Whereas high-P
metamorphism was initiated somewhat earlier in the GSB than
further west, as indicated by growth of metamorphic (granulite-
facies) zircon at 402 +0.8 Ma (O’Brien et al. 1997), subsequent
late Devonian HT– MP metamorphism in the GSB is well con-
strained by U– Pb monazite ages (van Breemen et al. 1988;
Bro
¨cker et al. 1998; Timmermann et al. 2000) and appears to be
contemporary with HP– LT metamorphism along the contact
zone of the Saxo-Thuringian and Tepla
´–Barrandian blocks
between 380 and 365 Ma.
Further west, recently obtained mid- to late Devonian dates for
the emplacement and metamorphism of the Lizard Peridotite and
associated rocks at the southern margin of the Cornubian Massif
(Sandeman et al. 2000; Nutman et al. 2001) reinforce the parallel
with the Giessen– Werra – Sudharz Ocean (Franke 2000), as the
latter also underwent contemporary metamorphism and defor-
mation. The latter has been interpreted as an obducted successor
basin to the Rheic Ocean.
In the Karkonosze– Izera complex (central West Sudetes) tec-
tonic exhumation was earlier and greater in the SE. This is
shown by: (1) early kinematic indicators in mylonitic ductile
shear zones (Mazur 1995; Seston et al. 2000); (2) decrease in
metamorphic grade from garnet zone in the SE to chlorite zone
in the NW (Baranowski et al. 1990; Kachlı
´k & Patoc
ˇka 1998;
Collins et al. 2000); (3) northwestward decrease of
40
Ar–
39
Ar
cooling ages (Marheine et al. 1999); (4) progressively later
flysch sedimentation onsets towards the NW. Also, late Devonian
unconformities in the central West Sudetes occur between the
Kłodzko metamorphic complex and the overlying Bardo Unit
(Hladil et al. 1998; Kryza et al. 2000), while Late Devonian and
Carboniferous coarse-grained clastic sedimentary deposits,
derived from exhumed metamorphic complexes to the east, were
deposited in syntectonic basins (Aleksandrowski & Mazur
2002). Deformation and metamorphism, which started in the
central West Sudetes in pre-late Devonian times (e.g. Hladil
et al. 1998) continued until the Tournaisian in both the northwes-
ternmost frontal parts of the West Sudetic orogenic wedge, where
me
´langes formed in the Kaczawa Complex (Collins et al. 2000),
and in the metamorphic core of the complex, as in the Orlica–
Snieznik area, where HP metamorphism produced eclogites.
This range of dates suggests that a series of small-scale collisional
events occurred, consistent with a progressive aggregation of the
constituent terranes of the ATA. In the West Sudetes Carbonifer-
ous metamorphism was followed by tectonic exhumation of
deeply buried crustal slices (353– 350 Ma) and the superimposi-
tion of a greenschist- to lower amphibolite-facies overprint
dated at 345– 340 Ma).
40
Ar–
39
Ar dating (325– 320 Ma) suggests
that metamorphism was complete by the mid- to late Carbonifer-
ous (Marheine et al. 2000), a timing supported by the age of depo-
sition in adjacent intramontane basins. These Carboniferous
events are generally considered to reflect the docking of the amal-
gamated ATA with the Avalonian and Bruno-Silesian margin of
the growing Laurussian supercontinent. The range of dates
suggests that collision was not a simple process: it probably
began earlier where the accreting ATA first impinged on promon-
tories, such as that of the Bruno-Silesian Massif, and occurred later
further west.
Deformation of Devono-Carboniferous sedimentary sequences
on the Laurussian passive margin in the Cornubian, Rhenish
and Bruno-Silesian massifs, as a result of this collision, produced
the only significant late Palaeozoic deformation to affect
both Avalonia and Bruno-Silesia. As the ATA approached Laurus-
sia, subduction was south-dipping beneath its leading edge,
causing the formation of an arc edifice preserved as volcanic
rocks of the Mid-German Crystalline High (MGCH), with its
associated oceanic back-arc basin, the Giessen– Werra – Su
¨dharz
‘ocean’. Subduction of this successor back-arc basin, which devel-
oped on the south side of the Rheic Ocean, occurred in Devono-
Carboniferous time, with obduction of fragments of it, originally
developed on the southern side of the ocean, eventually thrust
northwards across the Rheic Suture, so that they are now preserved
as ophiolitic outliers assigned to the Giessen – Werra – Su
¨dharz
or Selke Nappe (e.g. Franke 2000), north of the Rheic Suture.
Thus, the MGCH marks the superimposition of both late
Silurian–Devonian arc magmatism on the Avalonian margin
below the south-dipping Rheic Suture, and Carboniferous age vol-
canism above it (Oncken 1997). Small magnetic highs seem to
indicate a continuation of the volcanic centres within the MGCH
eastwards into Poland as far as a point just NE of the Leszno–
Wolsztyn High, corresponding to the location of the Moravian
Line.
Eastern extremities
As with Avalonia, the eastern extremities of the ATA abut the
Bruno-Silesian Massif (BSM), which must have still formed a
DETACHED TERRANE FRAGMENTS IN EEC 327
promontory on the Laurussian margin at the time of ATA accre-
tion. Without a perfect fit, the ATA presumably included crustal
blocks that converged with Laurussia further east, and that
might be expected to be accreted to the southern margin of the
BSM. However, because the latter margin is overthrust by the
Carpathian–Alpine Front, the mechanism for distribution of
ATA-related blocks further east is obscured. However, rocks
apparently subjected to Variscan-age metamorphism, often
intruded by mid-Carboniferous post-orogenic granitoids, occur
as basement inliers in the Carpathians, such as the Tatra Mts. In
the western Tatra Mts, metamorphic rocks containing amphi-
bolites with similar chemistry to those in the West Sudetes
(Gawe˛da et al. 2000) are cut by post-metamorphic Variscan
granitoid rocks, dated by both
40
Ar–
39
Ar and Rb– Sr methods at
300–330 Ma (Burchart 1968; Janak 1994). In the Romanian
Carpathians, the Getic– Supragetic basement (Iancu & Berza
2004) contains similar lithologies subjected to Variscan defor-
mation and metamorphism.
Further SE, the Balkan terrane exposed in western Bulgaria
(Fig. 1), and also sampled north of Sofia in the Svoge borehole,
contains mid-Ordovician faunas similar to those of Bohemia and
North Africa (Gutteriez-Marco et al. 2003), and typical of a
cold, peri-Gondwanan environment (Haydoutov & Yanev 1997).
Mid-Ordovician trilobites (Cyclopyge prisca) occur in shales over-
lain by Ashgill diamictites, indicating that the Balkan Terrane
remained attached to Gondwana in high latitudes long after
Avalonia had rifted off and migrated to lower latitudes. Built
upon a basement of Neoproterozoic ophiolites and Cambrian
calc-alkaline volcanic rocks, the thick Palaeozoic sequence also
includes Silurian argillites, Devonian clastic deposits and an
unconformity above the Lower Carboniferous units.
All these indicators point to an ‘ATA’ Gondwana affinity, with
collision with Moesia during the Carboniferous. However, the pre-
sence of a late Cambrian subduction-related sequence (493 Ma,
Carrigan et al. 2003) also needs explanation. Although this
could be interpreted as the product of intercontinental collision,
it could also be the result of a Cambrian arc–continent collision,
closing the intervening oceanic back-arc basin that had been
formed in the late Neoproterozoic. If so, the Balkan terrane
could represent yet another portion of the Neoproterozoic–
Cambrian supercontinent-fringing series of arcs and back-arc
basins. To the SE, the Balkan Terrane is structurally juxtaposed
with the Rhodope (Thracian) and Strandja terranes, which never-
theless seem to share its Palaeozoic continental affinities.
Still further east, in NW Turkey, the basement to the Sakarya
Zone shares a similar Palaeozoic history to blocks comprising
the ATA, in that it underwent Carboniferous metamorphism, fol-
lowed by intrusion of late Carboniferous post-orogenic granites
(Yilmaz et al. 1997). A rupture of the ATA, similar to that experi-
enced by Avalonia on collision with the Bruno-Silesian Promon-
tory, might explain, in the same way, the eastward migration of
displaced ATA-related blocks.
Why did Avalonia and the ATA separate
from Gondwana?
The composition of Palaeozoic magmatic rocks provides clues to
the causes of the separation of Avalonia and the ATA from the
Gondwana margin. In the northern Bohemian Massif extensive
bimodal magmatism occurred in the early Ordovician, with
bursts of magmatism continuing until the Devonian. Early,
mainly acidic magmatism of Cambro-Ordovician age (e.g.
Korytowski et al. 1993; Kro
¨ner et al. 1994; Philippe et al. 1995;
Hammer et al. 1997) shows calc-alkaline chemistry, which some
interpreted as evidence for an arc or active continent margin
tectonic setting (e.g. Oliver et al. 1993; Kro
¨ner & Hegner 1998).
Others suggested that the absence of supporting geological evi-
dence for an arc edifice at the time suggested that chemical
characteristics of the intrusions were inherited from extensive
melting of the calc-alkaline Panafrican basement (Kryza & Pin
1997; Aleksandrowski et al. 2000; Floyd et al. 2000). Subsequent,
dominantly basic volcanism was associated with clastic basin-fill
metasedimentary rocks, typical of magmatism associated with
an extensional tectonic setting. Minor associated felsic volcanic
rocks were shown by Sm– Nd systematics and their REE distri-
bution to result from continued melting of continental crust
(Furnes et al. 1994; Patoc
ˇka et al. 1997; Dostal et al. 2000),
whereas the compositional range of the basic rocks (e.g. Floyd
et al. 1996, 2000; Winchester et al. 1995, 1998) indicated magma
production resulting from the interaction of an enriched
plume with both asthenospheric and sediment-contaminated
lithospheric mantle sources (Floyd et al. 2000). Although the
preserved volume of magmatic rocks is smaller than younger
plume-influenced magmatic provinces, it has widespread correla-
tives in many parts of Western Europe, including the Massif
Central (Briand et al. 1991, 1995) and Massif des Maures
(B. Briand, pers. comm.) in France and NW Spain (e.g. Peucat
et al. 1990). Floyd et al. (2000) suggested that plume-induced
magmatism could also explain the amount of heat needed to
melt substantial volumes of lower crust to produce the major gran-
itoid bodies, this providing a possible mechanism for the fragmen-
tation of the Armorican Terrane Assemblage (ATA) as it separated
from Gondwana, and the repeated rifting of crustal fragments from
the Gondwana margin, including Avalonia and the ATA.
Palaeozoic palaeogeographical evolution and
accretions to the EEC
Recent reconstructions show that the main pre-Alpine, Central
European and related microcontinents formed an active continen-
tal margin (ACM) to the Pannotian supercontinent, with Avalonia
adjacent to the Amazonian Craton, based on the presence of inher-
ited 1.5 Ga ‘Rondonian’ ages obtained from rocks in Nova Scotia
(Nance & Murphy 1994) and central England (Tucker & Pharaoh
1991). To the east (present co-ordinates) the ACM extends
through the ATA (shown adjacent to the North African Craton
as it lacks inherited ‘Rondonian’ ages) and other blocks that are
thought to have separated from their peri-Gondwanan positions
later, notably the basements of Italy, the Pannonian blocks, and
the Tauride basement of southern Turkey. The presence of late
Neoproterozoic ophiolitic fragments within this ACM (e.g.
Yig
˘itbas¸ et al. 1999; Scarrow et al. 2001) attests to the obduction
of successor basins and suggests that the continental margin was
originally of West Pacific rather than Andean type.
Shared end-Proterozoic calc-alkaline magmatism and defor-
mation affecting all the accreted blocks records their former
location along an active margin to the end-Proterozoic superconti-
nent Pannotia. During the Cambrian, subduction along this margin
appears to have ceased or been greatly reduced, whereas during
the Tremadoc, renewed subduction resulted in calc-alkaline mag-
matism and the formation of large back-arc basins (the Gander Arc
and associated ophiolites) in the western part of the margin, now
preserved in Atlantic Canada. During the Llanvirn Stage,
bimodal acid– basic magmatism marks the detachment of Avalo-
nia, possibly as more than one block (Pharaoh 1999; Banka
et al. 2002; Winchester et al. 2002), marking the break-up of the
Gondwana margin, and renewed arc magmatism in the
‘Caradoc’ Stage (Exploits and Lake District arcs) marks its
rapid northward migration, narrowing the Iapetus Ocean. By this
stage, a widening Rheic Ocean opened between Avalonia and
the Gondwana margin, from which parts of the ATA were
already starting to rift as a series of linked blocks.
By the early Silurian, Avalonia had moulded itself onto the
TESZ margin of Baltica, with its easternmost extremity detached
and displaced eastwards along the southern margin of the new
J. A. WINCHESTER ET AL.328
supercontinent of Laurussia, comprising Avalonia, Baltica and
Laurentia. By this time also, many blocks of the ATA, already
rifted into an archipelago or related microcontinents, had separ-
ated from Gondwana, narrowing the Rheic Ocean, although the
widespread occurrence of late Ordovician glacial deposits
(lacking in Avalonia) indicates that significant separation from
Gondwana by even the earliest blocks occurred only after the
end of the Ordovician. However, the contrast between Silurian
microfaunas of the French Armorican terranes and those of the
Brabant Massif (Verniers 1982), suggests that the Rheic Ocean
remained broad. Subduction was initiated along the southern
margin of Avalonia, marking the earlier stage of volcanism in
the Mid-German Crystalline High. As terranes of the ATA
moved away from the Gondwana margin, the new seaway being
formed was the Proto-Tethys Ocean.
During the Devonian (Emsian), high-P, low-Tmetamorphism,
recording subduction and closure of intervening seaways within
the ATA, suggests that amalgamation of individual ATA terranes
had begun, eventually resulting in the production of a single ATA
microcontinent. Southward subduction, marked by renewed vol-
canism in the Mid-German Crystalline High, recorded the final
stage in the approach of the now-amalgamated ATA to Laurussia,
also impelled by Gondwanan convergence. Contact with the BSP,
still not firmly enough attached to Baltica to prevent some displa-
cement and relative rotation, was marked by dextral strike-slip
faulting along its western margin. This was followed by the
docking of most ATA blocks along the southern margin of Laur-
ussia. Easternmost parts of the ATA were detached on collision
with the BSP and displaced eastwards by sinistral faulting to
form the Variscide basement seen in Carpathian inliers, the
Balkan and Thracian terranes of Bulgaria, and the Sakarya and
Eastern Pontide crustal blocks of NW Turkey.
These investigations, and the collation of information, were supported by the
EU-funded PACE (Palaeozoic Amalgamation of Central Europe) TMR
Network, No. ERBFMRXCT97-0136. Part of the study is sponsored by the
FWO Research Project No. G.0094.01 ‘Tectonics of the Early Palaeozoic
basin development in NW Europe: basin analysis and magnetic fabric analysis
in the Belgian Caledonides’. The contribution of T.C.P. appears with permission
of the Executive Director, British Geological Survey (NERC). Particular thanks
are expressed to M. C. Go
¨ncu
¨og
˘lu (Turkey), I. Haydoutov and S. Yanev
(Bulgaria), A. Okay (Turkey), and A. Rushton (UK), who all provided valuable
additional data for inclusion.
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