Kinematics of the Alpine arc and the motion history of Adria

Platt, J. P.; Behrmann, Jan H.; Cunningham, P. C.; Dewey, John; Helman, Mark; Parish, M.; Shepley, M. G.; Wallis, Simon; Western, P. J.

doi:10.1038/337158a0

Cited by 178 publications

(77 citation statements)

References 32 publications

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“…General shortening was active in the same timespan on the western margin of the Po Plain and in the Northern Apennine. In particular, NE-SW to NW-SE directions of shortening detected in TPB sediments fit well with the post-Eocene pattern of NE-SW arc-normal transport direction of the Western Alpine arc proposed by Platt et al (1989), and with the NE-SW and NW-SE directions of shortening detected in the Ligurian Alps (close to the boundary with the Northern Apennine) by Hoogerduijn Strating et al (1991). The latter authors have suggested a possible superposition of two displacement directions of different ages, and in particular proposed a Late Miocene age for the NW-SE shortening related to the development of the Monferrato culmination (Hoogerduijn Strating et al 1991), supporting our data.…”

Section: Resultssupporting

confidence: 67%

Subsidence, stress regime and rotation(s) of a tectonically active sedimentary basin within the western Alpine Orogen: the Tertiary Piedmont Basin (Alpine domain, NW Italy)

Carrapa

Bertotti

Krijgsman

2003

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The Oligocene to Miocene Tertiary Piedmont Basin (TPB) is located in the NW part of Italy at the junction between the Apennine and the Alpine thrust belts. The position of the TPB on top of the Alpine/Apennine Orogen poses fundamental questions as to the tectonics of the basin subsidence. Having undergone little deformation, the TPB sediments provide an insight into the stress regime and rotations in the kinematically very complex area surrounding the basin itself. In this study we integrate subsidence and structural analysis with measurements of magnetic susceptibility anisotropy (AMS) and natural remanent magnetization (NRM) in order to better constrain the tectonic kinematics of the basin evolution. A major important period of subsidence occurred in the Middle Miocene involving the whole basin. During this period the TPB experienced NE-SW-directed compression and limited shortening. Some NW-SE-directed compressional features have been identified and they were probably active during post Tortonian times. Structures associated with north-south tension are quite common, but the amount of strain that they accommodate is minor. In addition this research provides new preliminary data suggesting counterclockwise rotation in the TPB by c. 20° which has taken place during Middle Miocene time.

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Section: Resultssupporting

confidence: 67%

Subsidence, stress regime and rotation(s) of a tectonically active sedimentary basin within the western Alpine Orogen: the Tertiary Piedmont Basin (Alpine domain, NW Italy)

Carrapa

Bertotti

Krijgsman

2003

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“…6, right part) shows how brutally the trends of stretching lineations and transport directions vary trough time. The anticlockwise rotation was pointed by Platt et al (1989a), but one can see more precisely a sharp ~90° change close to the Eocene-Oligocene boundary. Contrary to the coupled migration of the orogen and of the foreland basin during the Eocene lithospheric flexion ( fig.…”

Section: The Early Oligocene Orogenmentioning

confidence: 99%

Structural and sedimentary records of the Oligocene revolution in the Western Alpine arc

Dumont

Schwartz

Guillot

et al. 2012

Journal of Geodynamics

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“…(b) Scenario with subduction zone retreat manages to create space for crustal accretion without a need for retro-thrusting. (400-450 km) with that of the Carpathians (75-223 km; Platt et al 1989;Roca et al 1995;Schmid et al 1996;Nemčok et al 1999). The difference is also indicated by the fact that the entire upper crust of the more proximal parts of the European plate was accreted to the Alpine orogenic wedge, while involvement of the basement of the European plate in the West Carpathian accretionary wedge is minor (Roure et al 1993;Roca et al 1995;Schmid et al 1996;Nemčok et al 2000).…”

Section: Dynamic Setting Categories Of Thick-skin Provincesmentioning

confidence: 94%

Thick-skin-dominated orogens; from initial inversion to full accretion: an introduction

Němčok

Mora

Cosgrove

2013

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Fifty per cent of orogens have a thick-skin character, and have evolved from passive margin and intra-cratonic rift systems. One group of thick-skin provinces can be found at both pro-and retro-wedges of orogens associated with advancing subduction zones, that is, orogenic wedges whose advance vectors oppose the mantle flow. A second group can be found at prowedges of orogens associated with retreating subduction zones, that is, orogens whose advance vectors have the same direction as mantle flow. A third group is formed in intra-plate settings where mechanical strengthening is produced by internal shortening. Thick-skin province development is controlled by driving factors such as individual plate movement rates, overall convergence rates, orogen movement sense with respect to mantle flow, and pro-wedge v. retro-wedge location. These driving factors are themselves constrained by numerous internal and external factors. This introductory chapter focusses primarily on least-deformed case areas in order to understand the role of different factors in controlling the evolution of thick-skin tectonic provinces from the initial inversion stage to full accretion stage.Many thrust belts exhibit both thin-and thick-skin structural styles in different portions of the belt. Some thrust belts, such as the Andes, change style along-strike (Allmendinger et al. 1997;Baby et al. 2013; Carrera & Muñoz 2013;Iaffa et al. 2013;Moretti et al. 2013). Other thrust belts, such as the US Cordillera -Rocky Mountains, exhibit thin-skin structural styles in their interior and thick-skin style in their exterior (Hamilton 1988). A quick screening of the basic characteristics of orogens whose deformation styles are known (see Nemčok et al. 2005) shows that 50% of orogens have a thick-skin character. They have evolved from either passive margins or intra-cratonic rift systems. The most typical examples of the former (initial passive margin setting) are various Andean thick-skin provinces, the Tienshan and the Western Alps (Schmid et al. 1996(Schmid et al. , 1997Escher & Beaumont 1997 Each of these examples underwent a different portion of the complete deformation history of a thick-skin orogen, that is, from initial inversion to full accretion. An excellent introduction to this complete history can be found in Teixell & Babault (2013), who look at shortening across a number of orogens. They record a total shortening of 20 -25% across the High Atlas, 25-30% across the Eastern Cordillera of Colombia and about 40% across the Pyrenees. While Teixell & Babault (2013) reconstructed the complex deformation sequence in the Pyrenees and understood that mountain building comes from the numerous large-scale footwall edge short-cut faults through the rift margin, a less deformed record of the Eastern Cordillera allows one to see that a slow Paleocene -Eocene deformation was followed by the faster Oligocene-Early Miocene deformation and then by an accelerated deformation that took place since Late Miocene Silva et al. 2013). Work on the timing of ...

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Kinematics of the Alpine arc and the motion history of Adria

Cited by 178 publications

References 32 publications

Subsidence, stress regime and rotation(s) of a tectonically active sedimentary basin within the western Alpine Orogen: the Tertiary Piedmont Basin (Alpine domain, NW Italy)

Subsidence, stress regime and rotation(s) of a tectonically active sedimentary basin within the western Alpine Orogen: the Tertiary Piedmont Basin (Alpine domain, NW Italy)

Structural and sedimentary records of the Oligocene revolution in the Western Alpine arc

Thick-skin-dominated orogens; from initial inversion to full accretion: an introduction

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