Map view retrodeformation of an arcuate fold‐and‐thrust belt: The Jura case

Affolter, Thomas

doi:10.1029/2002jb002270

Cited by 59 publications

(121 citation statements)

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“…In the hanging wall of these solethrusts the sedimentary fill of the Molasse basin was passively translated NW-ward, uplifted and tilted to the NE (Laubscher 1961(Laubscher , 1992Guellec et al 1990;burkhard & sommaruga 1998;Affolter & Gratier 2004). Uplift and erosional unroofing of the external Alpine massifs accelerated around 10 Ma (Fü-genschuh & schmid 2003) and, thus, is compatible with an intra-tortonian onset of the main deformation phase of the JFtb.…”

Section: Late Miocene To Early Pliocene Folding Phase Of the Jura Moumentioning

confidence: 85%

“…Late Pliocene to present-day thick-skinned deformation of the Jura Mountains probably involves the activation of an intra-crustal detachment horizon that extends from the Alps beneath the Molasse basin into the Jura domain (Mosar 1999;Lacombe & Mouthereau 2002;Pfiffner 2006;Edel et al 2006;Ustaszewski & schmid 2007). the geodetic record, combined with geomorphologic evidence, indicates that the Eastern JFtb, which has accounted for up to 30 km of thinskinned shortening in its western parts during the last 9-10 million years (Philippe et al 1996;Affolter & Gratier 2004), is currently tectonically still active but deforms at very low horizontal displacement rates of less than 1 mm/y.…”

Section: Resultsmentioning

confidence: 99%

“…In its western, widest parts the JFtb accounts for 25-30 km shortening. this value decreases eastward to 13 km and 7 km in the Delémont and Aarau transects, respectively, and to 1 km in the Lägern anticline (Philippe et al 1996;Affolter & Gratier 2004).…”

Section: Geological and Topographic Setting Of The Area Addressedmentioning

confidence: 99%

“…It has accounted for up to 30 km of essentially thin-skinned shortening since late Miocene times (Laubscher 1961(Laubscher , 1992Philippe et al 1996;Affolter & Gratier 2004) and is still seismotectonically active (becker 2000; Lacombe & Mouthereau 2002;Edel et al 2006). the JFtb is flanked to the sE by the flexural swiss Molasse foreland basin of the Alps whilst its most external elements encroach on the bresse and Upper rhine grabens (Fig.…”

Section: Introductionmentioning

confidence: 99%

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Response of drainage systems to Neogene evolution of the Jura fold-thrust belt and Upper Rhine Graben

Ziegler

Fraefel

2009

Swiss J. Geosci.

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the eastern Jura Mountains consist of the Jura fold-thrust belt and the autochthonous tabular Jura and Vesoul-Montbéliard Plateau. they are drained by the river rhine, which flows into the North sea, and the river Doubs, which flows into the Mediterranean. the internal drainage systems of the Jura fold-thrust belt consist of rivers flowing in synclinal valleys that are linked by river segments cutting orthogonally through anticlines. the latter appear to employ parts of the antecedent Jura Nagelfluh drainage system that had developed in response to Late burdigalian uplift of the Vosgesback Forest Arch, prior to Late Miocene-Pliocene deformation of the Jura fold-thrust belt.the following stages are recognized in the evolution of the Jura Mountain drainage systems: 1) middle to late tortonian (10-7.2 Ma) folding-related overpowering and partial reversal of the south-directed Jura Nagelfluh drainage system, 2) Messinian to early Pliocene (7.2-4.2 Ma) Aare-Danube and protoDoubs stage, 3) early to middle Pliocene (4.2-2.9 Ma) Aare-Doubs stage, 4) late Pliocene to early Quaternary (2.9-1.7 Ma) Aare-rhine and Doubs stage and 5) Quaternary (1.7-0 Ma) Alpine-rhine and Doubs stage.Development of the thin-skinned Jura fold-thrust belt controlled the first three stages of this drainage system evolution, whilst the last two stages were essentially governed by the subsidence of the Upper rhine Graben, which resumed during the late Pliocene. Late Pliocene and Quaternary deep incision of the Aare-rhine/Alpine-rhine and its tributaries in the Jura Mountains and black Forest is mainly attributed to lowering of the erosional base level in the continuously subsiding Upper rhine Graben. Incision of the Doubs and Dessoubre canyons reflects uplift of the Franches-Montagnes and Franche-comté in response to thick-skinned deformation of the Jura fold-thrust belt, which had commenced around 3 Ma.Geodetic data indicate that uplift of the Jura Mountains, relative to the tabular Jura, presently continues at very low strain rates whilst the Upper rhine Graben subsides very slowly and the black Forest is relatively stable. Introductionthe Jura fold-thrust belt (JFtb), forming the core of the Jura Mountains, is the youngest and most external element of the central Alpine orogenic system. It has accounted for up to 30 km of essentially thin-skinned shortening since late Miocene times (Laubscher 1961(Laubscher , 1992Philippe et al. 1996;Affolter & Gratier 2004) and is still seismotectonically active (becker 2000;Lacombe & Mouthereau 2002;Edel et al. 2006). the JFtb is flanked to the sE by the flexural swiss Molasse foreland basin of the Alps whilst its most external elements encroach on the bresse and Upper rhine grabens ( Fig. 1; chauve et al. 1980;Dèzes et al. 2004).Evolution of the JFtb combined with the development of the Upper rhine Graben (UrG) and the bresse Graben, exerted strong control on the location of the repeatedly shifting watersheds between the rivers Danube, Doubs and rhine, which flow into the black sea, the Mediterran...

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Section: Late Miocene To Early Pliocene Folding Phase Of the Jura Moumentioning

confidence: 85%

Section: Resultsmentioning

confidence: 99%

Section: Geological and Topographic Setting Of The Area Addressedmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Response of drainage systems to Neogene evolution of the Jura fold-thrust belt and Upper Rhine Graben

Ziegler

Fraefel

2009

Swiss J. Geosci.

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“…Miocene and Early Pliocene imbrication and uplift of the External Massifs was accompanied by detachment and NW-translation of the Molasse Basin above an intraTriassic décollement horizon. This coincided with thinskinned deformation of the Jura fold-and-thrust belt some 50-80 km north of the front of the Alpine nappes (Buxtorf 1916;Laubscher 1961;Sommaruga 1997Sommaruga , 1999Affolter and Gratier 2004;Dèzes et al 2004). During Pliocene time, the Alpine deformation front, which also involved the basement, propagated northwestward into the Plateau Jura (Guellec et al 1990;Pfiffner et al 1997b;Ustaszewski and Schmid 2007).…”

Section: Evolutionmentioning

confidence: 99%

The last erosional stage of the Molasse Basin and the Alps

Schlunegger

Mosar

2010

Int J Earth Sci (Geol Rundsch)

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We present a synoptic overview of the Miocene-present development of the northern Alpine foreland basin (Molasse Basin), with special attention to the pattern of surface erosion and sediment discharge in the Alps. Erosion of the Molasse Basin started at the same time that the rivers originating in the Central Alps were deflected toward the Bresse Graben, which formed part of the European Cenozoic rift system. This change in the drainage direction decreased the distance to the marine base level by approximately 1,000 km, which in turn decreased the average topographic elevation in the Molasse Basin by at least 200 m. Isostatic adjustment to erosional unloading required ca. 1,000 m of erosion to account for this inferred topographic lowering. A further inference is that the resulting increase in the sediment discharge at the MiocenePliocene boundary reflects the recycling of Molasse units. We consider that erosion of the Molasse Basin occurred in response to a shift in the drainage direction rather than because of a change in paleoclimate. Climate left an imprint on the Alpine landscape, but presumably not before the beginning of glaciation at the Pliocene-Pleistocene boundary. Similar to the northern Alpine foreland, we do not see a strong climatic fingerprint on the pattern or rates of exhumation of the External Massifs. In particular, the initiation and acceleration of imbrication and antiformal stacking of the foreland crust can be considered solely as a response to the convergence of Adria and Europe, irrespective of erosion rates. However, the recycling of the Molasse deposits since 5 Ma and the associated reduction of the loads in the foreland could have activated basement thrusts beneath the Molasse Basin in order to restore a critical wedge. In conclusion, we see the need for a more careful consideration of both tectonic and climatic forcing on the development of the Alps and the adjacent Molasse Basin.

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Kinematics of Active Deformation Across the Western Kunlun Mountain Range (Xinjiang, China) and Potential Seismic Hazards Within the Southern Tarim Basin

et al. 2017

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The Western Kunlun mountain range is a slowly converging intracontinental orogen where deformation rates are too low to be properly quantified from geodetic techniques. This region has recorded little seismicity, but the recent July 2015 (Mw 6.4) Pishan earthquake shows that this mountain range remains seismic. To quantify the rate of active deformation and the potential for major earthquakes in this region, we combine a structural and quantitative morphological analysis of the Yecheng–Pishan fold, along the topographic mountain front in the epicentral area. Using a seismic profile, we derive a structural cross section in which we identify the fault that broke during the Pishan earthquake, an 8–12 km deep blind ramp beneath the Yecheng–Pishan fold. Combining satellite images and DEMs, we achieve a detailed morphological analysis of the Yecheng–Pishan fold, where we find nine levels of incised fluvial terraces and alluvial fans. From their incision pattern and using age constraints retrieved on some of these terraces from field sampling, we quantify the slip rate on the underlying blind ramp to 0.5 to 2.5 mm/yr, with a most probable long‐term value of 2 to 2.5 mm/yr. The evolution of the Yecheng–Pishan fold is proposed by combining all structural, morphological, and chronological observations. Finally, we compare the seismotectonic context of the Western Kunlun to what has been proposed for the Himalayas of Central Nepal. This allows for discussing the possibility of M ≥ 8 earthquakes if the whole decollement across the southern Tarim Basin is seismically locked and ruptures in one single event.

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Map view retrodeformation of an arcuate fold‐and‐thrust belt: The Jura case

Cited by 59 publications

References 49 publications

Response of drainage systems to Neogene evolution of the Jura fold-thrust belt and Upper Rhine Graben

Response of drainage systems to Neogene evolution of the Jura fold-thrust belt and Upper Rhine Graben

The last erosional stage of the Molasse Basin and the Alps

Kinematics of Active Deformation Across the Western Kunlun Mountain Range (Xinjiang, China) and Potential Seismic Hazards Within the Southern Tarim Basin

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