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Evolution of the Penninic Distal Domain

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Evolution of the Penninic Distal Domain EVOLUTION OF THE PENNINIC DISTAL DOMAIN By Sebastian Thronberens (283135) INHALTSVERZEICHNIS 1. Introduction .................................................................................................................................................... 3 1.1. Penninic Distal Domain .......................................................................................................................... 3 1.2. Depositinal Evolution ............................................................................................................................. 4 2. Tectonic Evolution .......................................................................................................................................... 6 3. Stratigraphy .................................................................................................................................................... 9 3.1. Valais-Trough ......................................................................................................................................... 9 3.2. Brianҫonnais terrane ............................................................................................................................. 9 3.3. Piemont-Ocean .................................................................................................................................... 10 4. Conclusion .................................................................................................................................................... 11 References ............................................................................................................................................................ 12 1. INTRODUCTION The Penninics constitute the only alpine tectonic unit extending along the whole alpine mountain belt. In the eastern Alps the penninic Rhenodanubian Flysh strikes from E to W. Further to the south the Tauern Window and the further west located Engadiner Window expose penninic units through Austroalpine nappes. In the central Alps the Penninics generally strike from NE to SW and build up the Prealps, separated geographically from the central penninic units and are located between the Molasse Basin and the Helvetics. In the western Alps the Penninics extend with N to S striking. FIG 1 TECTONIC MAP OF THE ALPS (SCHMID, FÜGENSCHUH ET AL. 2004). The Penninic domains derive from their paleogeographic depositional environments (Fig 1) and are separated into the lower Penninic nappes of the Valais-Trough, the middle Penninic Nappes of the Brianҫonnais domain and the upper Penninic nappes comprising depositions of the former Piemont- Ocean (Pfiffner et al. 2010).The stratigraphic units of the distal domains of the Piemont-Ocean and the Valais-Trough imply a relatively similar lithological sequence, which will be clarified in the ongoing chapters. 1.1. PENNINIC DISTAL DOMAIN The whole orogeny of the Alps and therefore the evolution of the penninic distal domain are a product of a classical Wilson cycle that started with the opening of the alpine Tethys between Eurasia in the north of Africa and Adria in Mesozoic times (Kissling 2008). It began with the breakup of the Pangaea Supercontinent which last from Triassic to early Cretaceous times. At the border of Jurassic to Triassic time. The alpine Tethys is subdivided in three large ocean basins along a large spreading zone, which also contains oblique striking transform faulting. FIG 2 PALGEOGRAPHICAL RECONSTRUCTION FOR THE LATE CRETACEOUS (SCHMID, FÜGENSCHUH ET AL. 2004). One of those transform faults strikes NW to SE along the western border of the former European continent and separates the Brianҫonnais and Corsica-Sardinia domain from the Iberian microplate, situated in the west (after a model from Frisch 1993). The Ligurian-Piemont- Ocean opens in the western part of the ridge, while the eastern part consists of the Penninic-Ocean. But depending on the literature the Penninic and Piemont-Ocean are expressions for the same domain and will be called the Piemont-Ocean in this paper. The alpine Tethys Ocean separates the European and the Adriatic continents. The Corsica-Sardinia and the Brianҫonnais microcontinents are located at the southern end of the European continent. In the south-east the Austroalpine is separated from the Brianҫonnais terrane by the Penninic Ocean (Fig 2). In the north of the Brianҫonnais domain, at the distal area of the European margin, the Valais-Trough is located, which rifting phase started during the late Jurassic, followed by spreading which is suggested to have lasted from Barremo-Aptian to Albo-Cenomanian with an aperture of 200 km for each phase (Stampfli and Mosar 1998). The rotation of Iberia from Turono to Senonian time is thought to have leaded to the closure of the Valais Ocean. 1.2. DEPOSITIONAL EVOLUTION In the Turonian time the distal domains of the Penninicum were located in deep oceanic areas, such as the Valais-Trough and the Piemont-Ocean. Even the Brainconnais continent seemed to be flooded in a shallow marine (pelagic) environment. Subduction under the Adriatic plate was certainly taking place. Induced by the subduction process, first alpine nappes were uplifted. Even the southern parts of the Piemont-Ocean have been concerned by the subduction. The erosion of the uplifted alpine nappes caused embankments into the Piemont-Ocean from south eastern direction, leaded to the deposition of the Gets-, Simme- and Arblatsch-Flysch. Those deposition set up the southern Penninic Flysch basin. The Brianconnais domain had pelagic conditions at that time. This was proven by the deposition of pelagic marly limestones at that time (source). The Valais-Trough was already filled with the Jurassic and Cretaceous Bündnerschiefer. During the Turonian the Prättigau Flysch started to deposit. From the northeast the Rhenodanubian Flysch got embanked into the basin. FIG 3 CROSS-SECTION THROUGH THE PREALPINE KLIPPEN NAPPES (PFIFFNER ET AL. 2010). Until the Eocene the subduction under the Adriatic continent propagated northward. The first distal european margin was subducted in such depth that it metamorphism processes took place. The Penninic Valais-Trough was part of one large basin complex located between the northern alpine foreland and the central Alps at that time. The basin comprised also the Helvetics and the Dauphinois and was a typical foreland basin created by the crustal bent caused by the overthrustig Adriatic continent, which also uplifted the alpine foreland and induced its erosion. Basin infill was delivered from south-western Alps creating the Niesen Flysch, but also from the central part of the Alps, depositing the Prättigau Flysch. The foreland basin is defined as the North Penninic Flysch basin. FIG 4 CROSS-SECTION OF WESTERN ALPS AND A SIMPLIFIED PALINSPASTIC MODEL (STAMPFLI & MOSAR 1998). In the Oligocene the Penninic domains were subducted and developed as nappe stack when first back thrusting induced by the continent-continent collision of the European and the African continent caused uplift of the nappe stacks. One part of the Penninic domain, comprising the Gets-, Simme- and Arblatsch Flysch got detached on an Mesozoic detachment horizon and was shifted northwards generating the Klippen nappe (Fig 3), while the other Penninic units got deeply subducted and were highly metamorphic overprinted. 2. TECTONIC EVOLUTION The Penninic domains are results of rift tectonics in the Alpine Tethys which seem to be related to the Pangaea break-up and the opening of the central Atlantic and might have started in late Triassic age. (Schmid et al. 1987; Hunziker et al. 1992). During the Jurassic the Alpine Tethys developed into subsiding rim basins with thinned cold lithosphere. Rifting, like the one causing the Valais- and Piemont-Ocean, separated the rim basins. The absolute beginning of this rifting phase is suggested to have occurred during the Sinemurian, followed by a thermal uplift phase in the Toarcian (Favre and Stampfli, 1992). Then a phase of seafloor spreading succeeded in the early-middle Jurassic (Bill et al. 1997). Except from the mentioned rim basins, thermal subsidence during the Bajocian led to progradation of carbonate platforms (Stampfli, 1998). So the former rift shoulders, including even the Brianҫonnais domain got sinked submarine as a result. In the late Jurassic the Iberian plate got separated from Newfoundland due to Atlantic rifting, what caused a rifting between France and the Brianҫonnais domain, the Valais rift, which is thought to have opened 200-350 km from late Jurassic to the Aptian (Stampfli, 1998). Thermal subsidence is suggested to have started in the Valanginian by Gradstein et al (1995). Further spreading is thought to have occurred from Barremo-Aptian to the Albo-Cenomanian and a closure of the Valais-Ocean during the Albian. Stampfli (1998) suggests an opening of the Valais-Ocean of 200 km during rifting and the same amount during the spreading phase. The closure was induced by the rotation of Iberia from Turono-Senonian time might have last till Lutetian time, proofed by age dating of sediment influx (Homewood, 1983). The following subduction caused the Valais domain to become the lower Penninic suture zone which got underplated below the northern part of the Brianҫonnais domain probably during the middle Eocene. The Brianҫonnais domain contains a crystalline basin which is set up of the Suretta and the Tambo nappes (Fig 4). Whereas the Suretta nappe is of pre-Alpine age and derived from an early Permian subvolcanic intrusion
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