Late‐stage deformation in a collisional orogen (Western Alps): nappe refolding, back‐thrusting or normal faulting?

Bucher, Stefan; Schmid, Stefan M.; Bousquet, Romain; Fügenschuh, Bernhard

doi:10.1046/j.1365-3121.2003.00470.x

Cited by 76 publications

(70 citation statements)

References 33 publications

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“…The younger ages presented in this study may represent this deformation, which was simultaneous with deformation along the Entrelor shear zone (Freeman et al, 1997) and the Mischabel back-fold (Barnicoat et al, 1995). These structures have been interpreted as a SEverging backfold and a backthrust, respectively (Barnicoat et al, 1995;Freeman et al, 1997), although contrasting structural observations from the Entrelor shear zone have also supported top-to-NW sense of shearing (Caby, 1996;Bucher et al, 2003).…”

Section: Exhumation Of the Gran Paradiso Massifmentioning

confidence: 62%

Dating deformation in the Gran Paradiso Massif (NW Italian Alps): Implications for the exhumation of high-pressure rocks in a collisional belt

Rosenbaum

Menegon

Glodny

et al. 2012

Lithos

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The Gran Paradiso massif, situated in the internal part of the Western Italian Alps, records a complex tectono-metamorphic history involving high-pressure metamorphism and subsequent exhumation during retrograde metamorphism. The exact timing of deformation and, consequently, the geodynamic evolution of this part of the Western Alps is still debated and is addressed here by the application of Rb/Sr geochronology, 40 Ar/ 39 Ar step heating and 40 Ar/ 39 Ar total fusion dating techniques. forming an extruding wedge. The kinematics associated with this wedge involved topto-W shearing within the Gran Paradiso nappe (e.g. Pont area shear zones) and top-to-E shearing at the top of the extruding wedge (e.g. Orco shear zone). Subsequent deformation (after ~34 Ma) was characterised by coaxial strain involving orogenicscale backfolding and backthrusting.

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Section: Exhumation Of the Gran Paradiso Massifmentioning

confidence: 62%

Dating deformation in the Gran Paradiso Massif (NW Italian Alps): Implications for the exhumation of high-pressure rocks in a collisional belt

Rosenbaum

Menegon

Glodny

et al. 2012

Lithos

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“…3) are also referred to as "Upper Penninic nappes". They occupy the structurally highest position within the Penninic nappe stack, unless their original position was severely modified by large-scale post-nappe folding (Schmid et al 1990;Bucher et al 2003;see Figs. 3a, b, and c).…”

Section: Piedmont-liguria Oceanmentioning

confidence: 99%

“…Other tectonic units attributed to this branch of the Alpine Tethys, particularly those of the Western Alps, comprise parts of the Piedmont-Liguria Ocean that stayed open until the onset of Tertiary collision, when the accretionary wedge of the Alpine subduction system collided with the Briançonnais ribbon continent (e.g. Schmid et al 1997;Stampfli et al 1998Stampfli et al , 2002Bucher et al 2003). In the Western Alps (but not in the Eastern Alps), Tertiary-age highpressure overprint of the Piedmont-Liguria units, together with adjacent parts of the most internal Briançonnais Terrane, is very widespread (Gebauer 1999;Frey et al 1999).…”

Section: Piedmont-liguria Oceanmentioning

confidence: 99%

“…The basement of the Mesozoic sediments of the Briançon-nais Terrane is preserved in the "Zone Houillère" (predominantly Late Carboniferous sediments, that were detached from their former Variscan basement; see Bucher et al 2003) and in basement nappes such as the Grand St. Bernard nappe system, and the Gran Paradiso and M. Rosa nappes of France, Italy and Western Switzerland (Figs. 3a, b), or the Tambo and Suretta nappes of Eastern Switzerland (Fig.…”

Section: Briançonnais Terranementioning

confidence: 99%

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Tectonic map and overall architecture of the Alpine orogen

Schmid¹,

Fügenschuh²,

Kissling³

et al. 2004

Eclogae geol. Helv.

Self Cite

1,082

1,015

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The new tectonic map of the Alps is based on the combination of purely structural data with criteria regarding paleogeographical affiliation and/or tectonometamorphic evolution. The orogenic evolution of the Alps is discussed using a combination of maps and paleogeographical reconstructions. It is proposed that the Alps are the product of two orogenies, a Cretaceous followed by a Tertiary one. While the former is related to the closure of an embayment of the Meliata ocean into Apulia, the latter is due to the closure of the Alpine Tethys between Apulia and Europe. The along-strike changes in the overall architecture, as for example revealed by geophysical-geological transects, are by far more substantial than hitherto believed. It appears that the Alps are still far from being over-investigated, as is demonstrated by many surprising recent findings based on field geology, laboratory results and geophysical methods of deep sounding. ZUSAMMENFASSUNGDie neue tektonische Karte der Alpen basiert auf einer Kombination von strukturellen Daten mit Kriterien der paläogeographischen Zugehörigkeit und/oder der tektono-metamorphen Entwicklung. Die Orogen-Entwicklung der Alpen wird anhand einer Kombination von Karten und paläogeographi-schen Rekonstruktionen diskutiert. Hierbei wird vorgeschlagen, dass die Alpen das Produkt von zwei Orogenesen sind: einer kretazischen, gefolgt von einer tertiären. Während erstere auf die Schliessung des Meliata-Ozeans zurückgeführt wird, ist letztere das Produkt der Schliessung der Alpinen Tethys zwischen Apulia und Europa. Die Änderungen in der Architektur der Alpen entlang dem Streichen sind weit wichtiger als bisher angenommen, wie am Beispiel geologisch-geophysikalischer Querschnitte illustriert wird. Es scheint, dass die Alpenforschung immer noch für Überraschungen gut ist. Dies zeigen neue Ergebnisse, die auf Feldforschung, Labormethoden und neue Methoden der geophysikalischen Tiefenerkundung abgestützt sind.

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“…On the other hand, the subducted lithospheric slab of the Western Alps remained attached to the European foreland. Continued Oligocene crustal shortening caused back folding of the West Alpine orogenic wedge and emplacement of nappes derived from the Valais Ocean, Brianc¸onnais Terrane and Piemont Ocean on the Dauphinois Shelf (Lickorish and Ford 1998;Fu¨genschuh and Schmid 2003;Bucher et al 2003). By end Oligocene times, the Alpine deformation front was located some 100 km to the south of the Upper Rhine Graben and about 100 km to the east of the Bresse Graben.…”

Section: Oligocene-early Miocene Main Rifting Stage Of Ecrismentioning

confidence: 99%

Evolution of the lithosphere in the area of the Rhine Rift System

Ziegler

Dèzes

2005

Int J Earth Sci (Geol Rundsch)

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The Rhine Rift System (RRS) forms part of the European Cenozoic Rift System (ECRIS) and transects the Variscan Orogen, Permo-Carboniferous troughs and Late Permian to Mesozoic thermal sag basins. Crustal and lithospheric thicknesses range in the RRS area between 24-36 km and 50-120 km, respectively. We discuss processes controlling the transformation of the orogenically destabilised Variscan lithosphere into an end-Mesozoic stabilised cratonic lithosphere, as well as its renewed destabilisation during the Cenozoic development of ECRIS. By end-Westphalian times, the major sutures of the Variscan Orogen were associated with 45-60 km deep crustal roots. During the Stephanian-Early Permian, regional exhumation of the Variscides was controlled by their wrench deformation, detachment of subducted lithospheric slabs, asthenospheric upwelling and thermal thinning of the mantlelithosphere. By late Early Permian times, when asthenospheric temperatures returned to ambient levels, lithospheric thicknesses ranged between 40 km and 80 km, whilst the thickness of the crust was reduced to 28-35 km in response to its regional erosional and local tectonic unroofing and the interaction of mantle-derived melts with its basal parts. Re-equilibration of the lithosphere-asthenosphere system governed the subsidence of Late Permian-Mesozoic thermal sag basins that covered much of the RRS area. By end-Cretaceous times, lithospheric thicknesses had increased to 100-120 km. Paleocene mantle plumes caused renewed thermal weakening of the lithosphere. Starting in the late Eocene, ECRIS evolved in the Pyrenean and Alpine foreland by passive rifting under a collision-related north-directed compressional stress field. Following endOligocene consolidation of the Pyrenees, west-and northwest-directed stresses originating in the Alps controlled further development of ECRIS. The RRS remained active until the Present, whilst the southern branch of ECRIS aborted in the early Miocene. Extensional strain across ECRIS amounts to some 7 km. Plume-related thermal thinning of the lithosphere underlies uplift of the Rhenish Massif and Massif Central. Lithospheric folding controlled uplift of the VosgesBlack Forest Arch.

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Late‐stage deformation in a collisional orogen (Western Alps): nappe refolding, back‐thrusting or normal faulting?

Cited by 76 publications

References 33 publications

Dating deformation in the Gran Paradiso Massif (NW Italian Alps): Implications for the exhumation of high-pressure rocks in a collisional belt

Dating deformation in the Gran Paradiso Massif (NW Italian Alps): Implications for the exhumation of high-pressure rocks in a collisional belt

Tectonic map and overall architecture of the Alpine orogen

Evolution of the lithosphere in the area of the Rhine Rift System

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