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 Lardeaux, Vojtech Janousek and Giacomo OggianoKarel Schulmann, José R. Martínez Catalán, Jean Marc formation of the European crustThe Variscan orogeny: extent, timescale and the

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The Variscan orogeny: extent, timescale and the formation

of the European crust

KAREL SCHULMANN1,2*, JOSE R. MARTINEZ CATALAN3, JEAN MARC LARDEAUX4,

VOJTECH JANOUSEK5 & GIACOMO OGGIANO6

1Center for Lithospheric Research, Czech Geological Survey, Klarov 3, 118 21,

Prague 1, Czech Republic2Ecole et Observatoire des Sciences de la Terre, Universite de Strasbourg,

UMR 7516 of CNRS, 1 Rue Blessig, 67084 Strasbourg, Cedex, France3Departamento de Geologıa, Universidad de Salamanca, 37008 Salamanca, Spain

4Geoazur, Universite Nice Sophia-Antipolis, 250 Rue A. Einstein,

Sophia-Antipolis, 06560 Valbonne, France5Czech Geological Survey, Klarov 3, Prague 11821, Czech Republic

6Universita di Sassari, Disbeg, Via Piandanna N84, 07100 Sassari, Italy

*Corresponding author (e-mail: schulmann.karel@geology.cz)

Hans Stille (1876–1966), probably the most influ-ential European geologist of the first half of thetwentieth century, defined four principal tectonicphases responsible for the formation of the VariscanOrogen in Europe (Stille 1920). The first, the BretonPhase, occurred during Late Devonian–early Car-boniferous time and was followed by the mostimportant orogenic deformation event, the SudeticPhase, which took place during early–late Carbon-iferous time. The younger deformation phases wererepresented by the Asturian (late Carboniferous)and Saalian (post-Carboniferous–early Permian)folding events. This chronological scheme wasbased on a sequence of deformation events definedby folding of stratigraphically well-constrainedsedimentary strata followed by angular unconfor-mity. Such an approach allowed the definition, to arelatively high precision, of the temporal and spatialextents of distinct crustal-scale deformation eventsthroughout the whole European Variscan belt.

This concept dominated European geologicalwisdom for over half a century and contributed sig-nificantly to a vision of short- and long-term episo-dic tectonic evolution of the Variscan continentalcrust (e.g. Matte 1986; Franke 1989). The episo-dicity of global tectonic events is supported bymodern geochronology which shows characteristicmajor peaks in U–Pb zircon age distributions(Condie et al. 2009). These peaks have been inter-preted in terms of variations in crustal growthrelated to episodic convection in the mantle (e.g.Arndt & Davaille 2013). However, plate tectonicsoffers a continuous scenario of crustal evolution

which is at odds with the observed episodic charac-ter of both crustal growth and tectonic activity(Sengor et al. 1993). Indeed, many researcherssuggest that U–Pb zircon age peaks are a functionof enhanced preservation of the continental crustrelated to the formation of large continental mas-ses (Hawkesworth et al. 2009). Similarly, the con-cept of tectonic phases was criticized and largelyabandoned at the end of the previous century aftergeneral acceptance of the plate-tectonic theoryand understanding of concepts of mechanical insta-bilities in structural geology and tectonics (e.g.Burg 1999).

Although the episodic nature of crustal growthcan be a matter for discussion, the regional super-position of tectonic events separated by periodsof quiescence is a reality which cannot be easilyexplained by different degrees of preservation.These distinct and regional deformation eventsresult from the accumulation of stress at plateboundaries resulting in catastrophic and short-livedtectonic deformation events that contribute to glo-bal mountain-building processes. In other words,changes in plate configurations may result in large-scale superposed deformations and recycling ofcrust which can be viewed as events or phases inorogenic evolution. The tectonic phases thereforeseem to reflect complete modification of plate-tectonic setting, resulting in distinct and discon-tinuous tectonic episodes which may be regardedas quasi-independent orogenic events.

In this book, a new pattern emerges showing thatthe Variscan evolution of continental Europe is not a

From: Schulmann, K., Martınez Catalan, J. R., Lardeaux, J. M., Janousek, V. & Oggiano, G. (eds)The Variscan Orogeny: Extent, Timescale and the Formation of the European Crust.Geological Society, London, Special Publications, 405, http://dx.doi.org/10.1144/SP405.15# The Geological Society of London 2014. Publishing disclaimer: www.geolsoc.org.uk/pub_ethics

at Indiana University Libraries on May 1, 2014http://sp.lyellcollection.org/Downloaded from

continuous process but that it resulted from severalmajor orogenic cycles which were not superim-posed in space and time. It is shown here that thenorthern Variscan realm is generally dominated bywell-characterized Late Devonian–Carboniferoustectono-metamorphic and magmatic events. Theserifting, subduction and collisional events are definedby sedimentary records, crustal growth, recyclingof continental crust and large-scale deformationsaffecting the bulk of western and central Europe.

However, the southern European crust shows adifferent picture as it was reworked by a majorlate Carboniferous–Permian collisional event,sometimes superimposed on previous Late Devo-nian and Carboniferous orogenic fabrics. The evi-dence for this late event is also preserved in thenorthern segment, but was apparently of signifi-cantly lower intensity compared to the south. It ismarked by localized magmatic recycling, exten-sional and transcurrent tectonic settings and devel-opment of localized sedimentary basins. It is notsurprising that the Variscan Orogen in westernand central Europe coincides spatially with mainareas affected by Breton and Sudetic phases, whilesouthern Europe is the locus of an Asturian tectonicevent. The three events do not reflect an episodicevolution of a single orogenic system, but in fact acomplete change in orientation of stress fields (e.g.Edel et al. 2013), thermal regime, degree of rework-ing and recycling of European crust. The expla-nation for such a dramatic switch in geometry ofdeformation on the scale of the European continentis a major change in plate configurations at the earlyand late Carboniferous boundary.

We hope that this volume will contribute tothe definition of the two major Variscan realmsresulting from two main and almost orthogonal oro-genic cycles and to the reconciliation of classicalEuropean geological wisdom with the plate tectonicparadigm. The papers are arranged to reflect theevolution of the European Variscan system in timeand space and to provide insight into the character-istic similarities and differences between individualtectonic, metamorphic and magmatic events acrossthe European continent.

The volume begins with the comparison of theVariscan evolution of the French Massif Centralwith the Vosges Mountains and the Bohemian Mas-sif (Lardeaux et al. 2014). These authors portraythe main differences and similarities between thetwo principal Variscan segments of central andwestern Europe by reviewing their crustal-scalearchitectures, specific rock associations and litho-tectonic sequences. Significant differences betweenthe internal (Moldanubian) Zone of the BohemianMassif and the French Massif Central are presented.It is shown that the French segment is formedby a Siluro-Devonian large-scale accretion system

developed prior to the main Carboniferous Vari-scan collision during northwards subduction ofthe Gondwanan margin. In contrast, the BohemianMassif was shaped by the opposite subduction ofthe Saxothuringian Ocean followed by continentalunderthrusting of the Saxothuringian plate, devel-opment of a continental arc and back-arc systemduring Late Devonian time and mixing of lower(Saxothuringian) and upper (Gondwana) plates ina large transitional zone during a collisional event.In a geological synthesis, Skrzypek et al. (2014)show that the Palaeozoic Vosges Mountains (NEFrance) represent a bridging area connecting thegeological structure of the Bohemian Massif to theeast with the French Massif Central in the west.These authors propose an evolutionary scheme inwhich the Northern Vosges represent a Rhenohercy-nian margin separated from the Tepla-Barrandiandomain by an early Carboniferous magmaticarc which is correlated with the Mid-GermanCrystalline Rise. However, the Saxothuringian–Moldanubian suture is thought to be obliterated bythe magmatic arc, while the Lalaye–Lubine Faultis interpreted as the Tepla-Barrandian–Moldanu-bian boundary. The Central Vosges are conse-quently compared with the Moldanubian domainof the Bohemian Massif where identical lithologiesrecord the Devonian–Carboniferous SE-directedsubduction of the Saxothuringian passive marginbelow the Gondwana-type upper plate. In thismodel, the Southern Vosges represent the upperMoldanubian crust and are linked to the southernBlack Forest.

A correlation between allochthonous unitsexposed in the NW Iberian Massif and the southernArmorican Massif by Ballevre et al. (2014) pro-vides further insight into the architecture of thewestern branch of the Variscan belt. This study,again based on lithological associations, structuralposition, age and geochemistry of protoliths andtectono-metamorphic evolution of critical units onboth sides of the Bay of Biscay, allows the definitionof Upper, Middle and Lower allochthonous thrustsheets overlying the Parautochthonous domain. Asin the French Massif Central, the Lower Allochthonrepresents a fragment of the outermost edge ofGondwana that underwent continental subductionshortly after the closure of a Palaeozoic oceanwhich is represented by the Middle Allochthon.The latter consists of supra-subduction ophiolitesand metasedimentary sequences alternating withbasic, mid-ocean ridge basalt (MORB) -type vol-canics. The opening of the oceanic domain wasrelated to the pulling apart of the peri-Gondwanancontinental magmatic arc, preserved as the UpperAllochthon. The origin of the Early Palaeozoic stra-tigraphic pile of autochthonous and parautochtho-nous units in NW Iberia is examined by Dias da

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Silva et al. (2014) using high-resolution U–Pbzircon geochronology. The aim of this study is tocorrelate both domains and establish their pre-and syn-orogenic Variscan evolution. The oldestbimodal volcanic suite yielded a late Cambrian age(c. 493 Ma), and the younger volcanics show petro-graphic, geochemical and age (c. 483 Ma) simi-larities to the volcano-detrital assemblage typicalof the autochthonous domain in northwestern andcentral Iberia. The geochemical signatures of bothvolcanic units suggest Cambro-Ordovician partialmelting of the northern Gondwana margin relatedto the opening of the Rheic Ocean. Ducassouet al. (2014) further refine accretionary and collisio-nal tectonic evolution of the Armorican segmentof the Variscan belt by U–Pb dating on zirconand 40Ar/39Ar on white mica. An Early Devonianunconformity is interpreted as the opening of aback-arc basin while 400 Ma magmatic zirconsrecord the emergence of a magmatic arc. Thisstage was followed by a Middle Devonian hiatusand disappearance of topographic relief duringLate Devonian time. However, the Devonian–Carboniferous boundary is marked by a uplift andcontinental sedimentation marking the progres-sive exhumation of Variscan metamorphic (micaat c. 350 Ma) and magmatic rocks (zircons atc. 390–340 Ma).

The magmatic evolution of the Bohemian Massifin the eastern branch of the Variscan belt is sum-marized by Zak et al. (2014). The authors recog-nize a Late Devonian–early Carboniferous growthof an inboard magmatic arc associated with orogen-perpendicular shortening due to the c. 354–346 Masubduction and continental underthrusting of theSaxothuringian domain. This event was followedby a collapse of the Tepla-Barrandian upper crustand exhumation of the high-grade (Moldanubian)core of the orogen at c. 346–337 Ma. Subsequently,the late readjustments within the amalgamatedBohemian Massif included crustal exhumation andc. 330–327 Ma mainly S-type granite plutonismalong the edge of the easterly (Brunian) continentalindentor and peripheral tectono-thermal activitydriven by strike-slip faulting and possibly mantledelamination until late Carboniferous–earliestPermian times. Middle Devonian–Permian mag-matic evolution characteristic of the Rhenohercy-nian active margin is examined by Tabaud et al.(2014) in the northern part of the Vosges Mountains.Major- and trace-elements and Sr–Nd isotopes forbasic to acidic magmatic rocks show that theyevolved from Middle Devonian tholeiitic to calc-alkaline volcanic sequences derived from partialmelting of a depleted mantle. Later calc-alkalinevolcanics (c. 334 Ma), diorite and granodioriteintrusions (c. 329 Ma) originated from enrichedmantle contaminated and metasomatized by fluids

expelled from a subduction zone. Finally, chemistryof high-K calc-alkaline granites (c. 318 Ma) sug-gests magma mixing between enriched mantle-derived melts and magmas from a young crustalsource, while the Mg–K granites (c. 312 Ma)might be related to partial melting of an enrichedmantle which has interacted with the crustalmelts. This evolution provides a complete magmaticrecord of the Rhenohercynian subduction cycledeveloped on Saxothuringian crust.

The tectono-metamorphic evolution of thesouthern branch of the European Variscan belt iscovered by a series of articles dealing with the geol-ogy of Spain, southern France and Italy. A groupof papers focused on Iberia and the Pyrenees illus-trates the contrasting tectonic, metamorphic andmagmatic evolution of this domain during the lateearly–late Carboniferous compared to the Varis-can Palaeozoic belt to the NE. Martınez Catalanet al. (2014) provide a synthesis of the Variscanmetamorphic evolution of the autochthonous do-main from NW and Central Iberia. These authorsshow that a Barrovian gradient is continuously fol-lowed by a low-pressure–high-temperature (LP/HT) metamorphism associated with the voluminousgranite magmatism. This evolution is explained bycrustal thickening resulting from the Gondwana–Laurussia collision followed by a period of thermalrelaxation and a long-lasting extensional stage. Theauthors propose that the Central Iberian oroclineis a late feature which had no significant effecton the metamorphic evolution and only controlledthe present localization of gneiss domes and grani-toids. The authors claim that the role of mantledelamination in thermal evolution of the Iberiansector of the Variscan belt was only moderate.Carreras & Druguet (2014) propose that lateCarboniferous tectonic evolution of NE Iberiawas marked by significant differences betweenthe northern internal zone with high-grade meta-morphic rocks, structural domes and syntectonicplutons, and the south where unmetamorphosedand low-grade rocks are present along with unde-formed late- to post-tectonic plutons. The authorssuggest that such a distribution contradicts existingmodels where this part of the Variscan belt waslocated in an external foreland. Variscan orogenicfabrics provide evidence for bulk transpressiongradually evolving from a NNW–SSE-directedcrustal shortening to NW–SE wrench-dominatedtectonics. The LP/HT metamorphic peak andmagmatism coincided with the latest stages ofthe NNW–SSE event. The timing of crustal-scaledeformations including crustal flow and gneissdome formation in the Pyrenees is synthesizedby Denele et al. (2014). It is shown that after amoderate upper crustal thickening between 323and 308 Ma, the Variscan segment of the Pyrenees

INTRODUCTION

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experienced crustal flow at c. 306 Ma and gneissdome formation at c. 304 Ma. Localization ofthe deformation along reverse-dextral shear zonesoccurred at c. 300 Ma. The authors propose thatthe development of the Pyrenean orogenic seg-ment was contemporaneous with the formation ofthe Cantabrian Orocline and, in contrast to MartınezCatalan et al. (2014), suggest a possible strong influ-ence of mantle delamination for such a short-livedthermal evolution of the belt.

The Variscan massifs in southern France areinterpreted as having resulted from long tectono-thermal collisional evolution terminated by a majorlate Carboniferous HT event. Even if the earlyorogenic stages are different compared to Iberianand Pyrenean examples, the HT compressive eventwas similar (if not identical) for the whole southEuropean Variscan belt. Such an evolution is exem-plified by the migmatitic dome of the MontagneNoire (Faure et al. 2014). These authors providenew geochronological data from mafic eclogiteswhich yield zircon and rutile U–Pb SIMS ages ofc. 315–308 Ma. However, the 357–352 Ma Sm–Nd age for the same rock and monazite chemicalU–Th–Pb (CHIME) ages from relict grains in theAxial Zone kinzigites may indicate an earlier agefor the HP event. These ages agree with CHIMEages of 340–320 Ma obtained from the metamor-phic envelope of the dome. These data are incor-porated in a crustal-scale model suggesting anorth-directed intracontinental subduction respon-sible for the HP/LT Late Devonian–early Carbon-iferous metamorphism, coeval with kilometre-scalesouth-vergent recumbent folds in the Palaeozoicnon-metamorphic cover. This event was followedby the development of the Axial Zone migmati-tic dome at 330–320 Ma, and upright folding inthe Palaeozoic non-metamorphic series. A broadlysimilar pattern is proposed for the tectonic andmetamorphic evolution of the Maures–TanneronMassif further east (Schneider et al. 2014). Themodel accounts for Siluro-Devonian subductionassociated with HP/LT metamorphism, subsequentCarboniferous nappe stacking and back-thrusting.Nappe stacking and back-thrusting were associatedwith typical Barrovian metamorphism which poss-ibly started at 360 Ma and progressively evolvedto higher-temperature metamorphism during 330–300 Ma in the internal part of the belt. Continuouscompressive forces applied to the belt allowed ver-tical extrusion of the orogenic root in fold-domestructures and late Carboniferous orogen-paralleltranspressive shearing.

The final evolution of the Variscan belt in south-ern Europe is documented by two papers describingthe transition during late Carboniferous–Permo-Triassic time. Palaeomagnetic investigations of theCorso-Sardinian block and Maures–Esterel Massif

(Edel et al. 2014) show a change in magneticorientation during the late Carboniferous–earlyPermian period (305–280 Ma). This trend is inter-preted in terms of a large-scale 908 clockwise rota-tion of the southern branch of the Variscan belt thatmatches the successive change in shortening direc-tions revealed by structural geology. The chro-nological match between the palaeomagnetic andtectonic datasets is interpreted as a result of large-scale dextral wrench movements in the lithospherebetween Gondwana and Laurussia similar to thoseproposed by Carreras & Druguet (2014) or Deneleet al. (2014). The evolution of the southern Variscanbranch in the southern Alps is discussed by Spallaet al. (2014), who propose that the continentallithosphere was thermally and mechanically per-turbed during the Variscan subduction and colli-sion. Here, diffuse igneous activity accounting foremplacement of huge gabbro bodies was associatedwith HT metamorphism during Permian–Triassictime. Two-dimensional finite-element modelling isapplied to examine the transition between the lateVariscan orogenic evolution and Permian–Triassiclithospheric thinning heralding the opening of theTethys Ocean. A comparison of model predictionswith a broad set of natural data suggests that thelate collisional gravitational collapse does not fitnatural observations. Instead, an active extensionis proposed to satisfy model predictions, extensivepartial melting of mantle and the exceptionally elev-ated HT regime.

This is a contribution to the LK11202 programme of theMinistry of Education of the Czech Republic (awardedto KS).

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