Some overall aspects of Jura dynamics

Laubscher, H. P.

doi:10.2475/ajs.272.4.293

Cited by 88 publications

(62 citation statements)

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“…As most of these normal faults occur near the Morez and the Vuache tear Faults (7 and 9 in Fig. 3), this local extension could reflect the thrustparallel stretching during the fold-and-thrust tectonics required by the divergence of the displacement vectors within the belt (Laubscher, 1972;Hindle and Burkhard, 1999). However, we find it unlikely as no normal slips coeval or postdating folding have been observed.…”

Section: The Minor Ne -Sw Extensioncontrasting

confidence: 46%

“…7). This stress distribution has been recognized early by the pioneer Jura workers (e.g., Laubscher, 1972;Plessmann, 1972). Other workers (Fig.…”

Section: Stress Deflections Indicate Crustal Heterogeneitiesmentioning

confidence: 96%

“…The two stress regimes are thus related through r 2 /r 3 stress permutation. Such r 2 /r 3 stress permutation is explained by Laubscher (1972) by a decrease in the horizontal stress perpendicular to displacement (that is approximately parallel to fold axis) due to necessary stretching related to the divergence of displacement trajectories within the arcuate belt. Stretching is accommodated by tear faults where the horizontal stress parallel to fold axes has been converted from r 2 (reverse regime) to r 3 (strike-slip regime).…”

Section: Stress Regimesmentioning

confidence: 99%

“…Deformation was active from about 10 to 5 Ma ago and is referred to as the ''Jura Phase'' or the Late Miocene tectonics (for a review, see Burkhard, 1990;Laubscher, 1992). Early deformation in the Jura Mountains has been locally identified (e.g., Mathis, 1974;Laubscher, 1972Laubscher, , 1986Chauve et al, 1988), but the detailed fracture pattern and corresponding stress fields have not been considered for the whole Jura Mountains. In addition, origin of pre-orogenic deformation in the Jura and in neighboring areas is controversial (Sopena and Soulas, 1973;Illies, 1975;Buchner, 1981;Bergerat and Geyssant, 1987;Homberg et al, 1994).…”

Section: Introductionmentioning

confidence: 99%

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Structural inheritance and cenozoic stress fields in the Jura fold-and-thrust belt (France)

et al. 2002

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Based on an analysis of 8000 minor fault-slip data in the Jura Mountains (France), we discuss the influence of pre-existing discontinuities on the development of fold-and-thrust belts. We present palinspastic maps showing the stress fields and active faults during the Cenozoic pre-orogenic events in the Jura belt prior to the main Late Miocene fold-and-thrust tectonics. During the Eocene, a N -S strike-slip regime produced a few NNE -SSW sub-vertical strike-slip faults in the central external Jura and a few E -W reverse faults in the eastern Jura near the future frontal thrust. During the Oligocene, an average WNW -ESE extension, with irregular stress trajectories, resulted in normal faulting along N -S to NE -SW trends in the external part of the belt, WNW -ESE trends along the future northern and northeastern frontal thrust, and NW -SE trends in the internal Jura. The Late Miocene tectonics began with a strike-slip regime with a fan-shaped compressional trajectory. It was followed by a stress field with similar stress direction, but local r 2 /r 3 stress permutation resulted in strike-slip regime domains contrasting with reverse regime domains. Stress deflections and permutations occurred near inherited cover and basement discontinuities. Major deformation zones, like the Jura frontal thrust onto the foreland, the thrust of the internal central Jura onto the external Jura, and the narrow deformation bands within the flat-lying plateaus formed close to the inherited faults. The structural style of the Jura belt thus partly mimics the pre-orogenic fault pattern. Stress deflections point to the pre-orogenic faults, express the indentation process of the Jura by its hinterland, and highlight successive slip events along major faults during the fold-and-thrust tectonics. This case study illustrates the relevance of minor fault-slip studies for characterizing both the pre-orogenic tectonics and the kinematics of the deformation. D

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Section: The Minor Ne -Sw Extensioncontrasting

confidence: 46%

“…7). This stress distribution has been recognized early by the pioneer Jura workers (e.g., Laubscher, 1972;Plessmann, 1972). Other workers (Fig.…”

Section: Stress Deflections Indicate Crustal Heterogeneitiesmentioning

confidence: 96%

Section: Stress Regimesmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Structural inheritance and cenozoic stress fields in the Jura fold-and-thrust belt (France)

et al. 2002

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“…This Late Paleozoic trough system is commonly held responsible for nucleating a Paleogene-age continental transfer zone between the URG in the NE and the Bresse Graben in the SW. This so-called Rhine Bresse Transfer Zone linked the simultaneous opening of the two graben systems by sinistral transtensive reactivation of ENE-oriented basement faults of the pre-existing Permo-Carboniferous trough system (Laubscher 1972(Laubscher , 1973Bergerat & Chorowicz 1981;Illies 1981;Ziegler 1992;Lacombe et al 1993;Ustaszewski et al 2005a,b). Giamboni et al 2004a).…”

Section: Geological Setting and Previous Workmentioning

confidence: 99%

Latest Pliocene to recent thick-skinned tectonics at the Upper Rhine Graben – Jura Mountains junction

2007

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The southernmost Upper Rhine Graben and adjacent Jura experienced basement-rooted shortening that occurred after the deposition of the Pliocene fluvial "Sundgau gravels". Folds affecting the base of these gravels systematically trend NE to ENE. Combined evidence from reflection seismic lines and contour maps of the base-Tertiary and base-Pliocene levels indicates that these folds probably formed by thick-skinned reactivation of both NNE-SSW and WSW-ENE-striking faults. This thick-skinned shortening is NW-SE oriented, i.e. parallel to the maximum horizontal stresses inferred from seismotectonics. NNE-SSW-striking faults (paralleling the Upper Rhine Graben) have been reactivated in sinistral strike-slip mode. However, dextrally transpressive reactivation of the WSW-ENE-trending faults that belong to the Rhine-Bresse Transfer Zone is interpreted to predominate.Deflections of recent river courses around the crests of en-échelon-aligned surface anticlines suggest that the deformation is ongoing at present.Retro-deformation of the folds affecting the base of the Sundgau gravels indicates horizontal displacement rates of about 0.05 mm/a. This corresponds to a minimum strain rate in the order of 2·10 -16 s -1 , given the maximum time span of 2.9 Ma for this deformation, i.e. the biostratigraphically determined minimum age of the gravels. A change from thin-skinned tectonics, that prevailed during the main phase of Jura folding, to very probably still ongoing thick-skinned tectonics is inferred to have occurred in the Late Pliocene. We speculate that this change might be linked to the incipient inversion of Permo-Carboniferous troughs within the Alpine foreland in general. This inversion in dextrally transpressive or purely compressive mode along a WNW-ESE-trending basement fault, that is part of the Rhine-Bresse Transfer Zone, which in turn was prestructured during the formation of the Permo-Carboniferous troughs, could have triggered the 1356 Basel earthquake.

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Lithologic Effects on Landscape Response to Base Level Changes: A Modeling Study in the Context of the Eastern Jura Mountains, Switzerland

et al. 2017

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Landscape evolution is a product of the forces that drive geomorphic processes (e.g., tectonics and climate) and the resistance to those processes. The underlying lithology and structural setting in many landscapes set the resistance to erosion. This study uses a modified version of the Channel‐Hillslope Integrated Landscape Development (CHILD) landscape evolution model to determine the effect of a spatially and temporally changing erodibility in a terrain with a complex base level history. Specifically, our focus is to quantify how the effects of variable lithology influence transient base level signals. We set up a series of numerical landscape evolution models with increasing levels of complexity based on the lithologic variability and base level history of the Jura Mountains of northern Switzerland. The models are consistent with lithology (and therewith erodibility) playing an important role in the transient evolution of the landscape. The results show that the erosion rate history at a location depends on the rock uplift and base level history, the range of erodibilities of the different lithologies, and the history of the surface geology downstream from the analyzed location. Near the model boundary, the history of erosion is dominated by the base level history. The transient wave of incision, however, is quite variable in the different model runs and depends on the geometric structure of lithology used. It is thus important to constrain the spatiotemporal erodibility patterns downstream of any given point of interest to understand the evolution of a landscape subject to variable base level in a quantitative framework.

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Some overall aspects of Jura dynamics

Cited by 88 publications

References 0 publications

Structural inheritance and cenozoic stress fields in the Jura fold-and-thrust belt (France)

Structural inheritance and cenozoic stress fields in the Jura fold-and-thrust belt (France)

Latest Pliocene to recent thick-skinned tectonics at the Upper Rhine Graben – Jura Mountains junction

Lithologic Effects on Landscape Response to Base Level Changes: A Modeling Study in the Context of the Eastern Jura Mountains, Switzerland

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