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Laurussia and the Juxtaposition and the (Helvetic, Penninic, Austroalpine, Southalpine) Relics in the Alps

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Laurussia and the Juxtaposition and the (Helvetic, Penninic, Austroalpine, Southalpine) Relics in the Alps Published in "%XOOHWLQRIWKH*HRORJLFDO6RFLHW\RI$PHULFD " which should be cited to refer to this work. Pre-Mesozoic Alpine basements— Their place in the European Paleozoic framework Jürgen F. von Raumer1,†, François Bussy2,†, Urs Schaltegger3,†, Bernhard Schulz4,†, and Gérard M. Stampfl i2,† 1Département de Géosciences, Université de Fribourg, 6, Chemin du Musée, CH-1700 Fribourg, Switzerland 2Earth Sciences Institute (ISTE) Geopolis, CH-1015 Lausanne, Switzerland 3Section des Sciences de la Terre et de l’Environnement, Université de Genève, rue des Maraîchers 13, Ch-1205 Genève, Switzerland 4Institut für Mineralogie, Brennhausgasse 14, D-09596 Freiberg/Sachsen, Germany ABSTRACT tinction of the former tectonic lower-plate Alpine deformational chain (von Raumer and situation is traceable but becomes blurred Neubauer , 1993) from their Mesozoic sedimen- Prior to their Alpine overprinting, most of through the subsequent oblique subduction tary envelopes. After Zwart and Dornsiepen the pre-Mesozoic basement areas in Alpine of Paleo tethys under Laurussia accompanied (1978) and Rast and Skehan (1983) considered orogenic structures shared a complex evolu- by large-scale strike slip. the general relationship between European and tion, starting with Neoproterozoic sediments Since the Pennsylvanian, this global col- transatlantic Cadomian basement areas, Ziegler that are thought to have received detrital lisional scenario has been replaced by sub- (1984) proposed a peri-Gondwanan origin for input from both West and East Gondwanan sequent and ongoing shortening and strike some of the Alpine basement’s constituents. cratonic sources. A subsequent Neoprotero- slip under rising geothermal conditions, and Stampfl i (1996) developed the fi rst theoretical zoic–Cambrian active margin setting at the all of this occurred before all these puzzle approach for a global geodynamic interpretation Gondwana margin was followed by a Cam- elements underwent the complex Alpine of this polyorogenic domain. In his defi nition brian–Ordovician rifting period, including reorganization. of the “intra-Alpine” basement, he illustrated an Ordovician cordillera-like active margin the complex global geodynamics bound to the setting. During the Late Ordovician and Si- INTRODUCTION evolution of the oceanic margins at the northern lurian periods, the future Alpine domains re- Gondwana margin during late Paleozoic evo- corded crustal extension along the Gondwana In the more than 200 yr of identifi cation of lution. The corresponding plate-tectonic evolu- margin, announcing the future opening of pre-Mesozoic basement elements in the Alpine tion of the Alpine domain after Late Permian the Paleotethys oceanic domain. Most areas orogen, Ebel (1808) was the fi rst to display times has recently been revealed (Stampfl i and then underwent Variscan orogenic events, in- the Alpine basement areas and outcrops of the Hochard, 2009). This palinspastic interpretation cluding continental subduction and collisions northern foreland with the same color; Desor also enabled the recognition of the original pre- with Avalonian-type basement areas along (1865) defi ned the Alpine basement realms Alpine situation of the pre-Permian basement http://doc.rero.ch Laurussia and the juxtaposition and the (Helvetic, Penninic, Austroalpine, Southalpine) relics in the Alps. duplication of terrane assemblages during in their Alpine framework; and Niggli (1960) Although many parts of the basement were strike slip, accompanied by contemporane- fi rst outlined the contours of the Alpine over- highly overprinted during the Alpine metamor- ous crustal shortening and the subduction of print on the basement by mapping the zoned phic events, some areas (e.g., in the External Paleotethys under Laurussia. Thereafter, the distribution of characteristic Alpine metamor- massifs) were less affected, making it possible fi nal Pangea assemblage underwent Triassic phic minerals, evolving from the lowermost to recognize older lithologies and structures. and Jurassic extension, followed by Tertiary greenschist facies in the north to the amphibolite The aims of this paper are to summarize shortening, and leading to the buildup of the facies to the south. what is actually known about the pre-Mesozoic Alpine mountain chain. The intensive geological field work per- Alpine basement and to compare known pre- Recent plate-tectonic reconstructions formed by many groups between the cities of Mesozoic Alpine basement units (Figs. 1 and 2) place the Alpine domains in their supposed Graz (Austria) and Genova (Italy) led to the with the observed lithostratigraphic units of initial Cambrian–Ordovician positions in detailed reconnaissance of the Alpine colli- the larger Variscan framework. To this end, it the eastern part of the Gondwana margin, sional belt (e.g., Trümpy et al., 1980; Hunziker is necessary to repeat certain previously pub- where a stronger interference with the Chi- et al., 1992; Pfi ffner et al., 1996; Frey et al., lished details. Consequently, we must describe nese blocks is proposed, at least from the 1999; Schaltegger and Gebauer, 1999; Ober- the Paleozoic evolution of the future Alpine do- Ordo vician onward. For the Visean time of hänsli, 2004; Schmid et al., 2004; Handy et al., mains located at the interface of the super conti- the Variscan continental collision, the dis- 2010) and the complex imbrication of pre- nents: Gondwana in the south and Laurussia in Mesozoic basement blocks through large-scale the north. The geodynamic reconstruction of nappe and strike-slip tectonics (Escher et al., the Alpine basement areas has much in com- † E-mails: [email protected]; francois mon with crystalline basement areas of Central [email protected]; [email protected]; Bernhard 1997; Stampfl i, 2001; Steck et al., 2001). This [email protected]; Gerard.Stampfl i@ long-lasting research permitted the separation Europe and is regarded in the light of the newest unil.ch of pre-Permian basement relics hidden in the plate-tectonic reconstructions (Stampfl i et al., of the Rheic Ocean (ca. 480 Ma) and collided with Baltica, the Hunic terranes (e.g., Karakum, SX Kunlun East, Pamir-Jinsha, Qaidam, Qilian, M Turan; cf. von Raumer and Stampfl i, 2008), Arm Alps which were formerly located at the eastern con- tinuation of Avalonia, separated from the Gond- MC wana margin during the opening of the eastern branch of the Rheic Ocean. They subsequently collided with the northern Chinese blocks and WL Py Co not with the Laurussia margin, as previously Aq Ca argued (Stampfl i and Borel, 2002). CIb Sa Like most of the European basement areas of Variscan age, those of the Alpine realm were OM believed to have a north Gondwanan origin (von Si SP Raumer, 1998), and the following evolution was proposed (e.g., Neubauer, 2002; Neubauer et al., 2002; Schätz et al., 2002; Stampfl i et al., 2002; von Raumer et al., 2002): Figure 1. The pre-Mesozoic basement areas of the Alps (brown) and (1) An active margin setting developed along their present-day locations among the Central European Variscan base- the north Gondwana margin during the Neo- ment areas (light orange) and Avalonian basements (pink). Terrane map proterozoic–Early Cambrian period contempo- with subdivision into geodynamic units (modifi ed after Stampfl i et al., raneous with the Cadomian orogenic evolution 2006) (yellow), inspired by Franke (1989). For a better understanding (a compilation of ages is shown in Schaltegger, and identifi cation, the contours of the specifi c geodynamic units are 1997a; Schulz, 2008; see Fig. 3). used in the reconstructions. Aq—Aquitaine; Arm—Armorica; Ca— (2) When the Rheic Ocean opened along the Cantabrian terrane; CIb—Central Iberian; Co—Corsica; M—Molda- western margin of Gondwana, its eastern mar- nubian Units; MC—French Central Massif ; OM—Ossa Morena; gin, which was more or less the site of the future Py—Pyrenees; Sa—Sardinia; Si—Sicilian-Apulian basements; SP— Alpine basement areas, underwent a complex South Portuguese; SX—Saxothuringia; WL—West Asturian–Leonese and not yet suffi ciently resolved Ordovician zone. Blue lines—Geographic boundaries. evolution, including signatures of intra-arc magmatism with extension, subduction-colli- sion, and the subsequent opening of the eastern 2011), which present constraints for new inter- the geological data were always put forward, at branch of the Rheic Ocean. pretations of its geodynamic evolution. a certain stage the model enables choices based (3) A passive margin setting developed after One of the major diffi culties encountered on plate-tectonic principles. the Late Ordovician, and the crustal exten- when comparing pre-Mesozoic Alpine base- Consequently, the placing of Alpine base- sion lasted until the opening of the Paleotethys ments with those outside the Alps is the Alpine ment areas in their former framework follows Ocean during the Devonian. metamorphic overprint masking all the older very different constraints and represents the http://doc.rero.ch structures. A strong understanding of basements major task of this paper, but this analysis will Precambrian Evolution outside the Alps must be accompanied by a rec- be subject to change when new data introduce ognition of the corresponding structures in the new constraints. Frisch and Neubauer (1989) fi rst presented Alpine domain. It is also evident that these recon- the concept of a Neoproterozoic–early Paleozoic structions have profi ted from the input of many PLATE-TECTONIC active margin setting in the Penninic and Austro- new ages and geochemical
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