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The Geometry and Evolution of the Jura Mountains: Fernschub Mechanics

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The Geometry and Evolution of the Jura Mountains: Fernschub Mechanics The Geometry and Evolution of the Jura Mountains: Fernschub mechanics Tabea Kleineberg 03.10.2013 Paper for the excursion “Geländeseminar Alpen” led by Prof. Dr. Janos Urai, Institute of Structural Geology, Tectonics and Geomechanics and Prof. Dr. Ralf Littke, Institute of Geology and Geochemistry of Petroleum and Coal at the RWTH Aachen University. 2 The Geometry and Evolution of the Jura Mountains: Fernschub mechanics Tabea Kleineberg 319001 ABSTRACT .......................................................................................................................................3 1. GEOLOGICAL SETTING..................................................................................................................4 2. STRATIGRAPHY AND EVOLUTION OF THE JURA MOUNTAINS.......................................................5 2.1 BASEMENT .......................................................................................................................................5 2.2 THE SEDIMENT COVER ........................................................................................................................5 2.2.1 The basal décollement within the Triassic evaporites ...........................................................7 2.3 EVOLUTION OF THE JURA MOUNTAINS..................................................................................................7 2.4 PALINSPASTIC RECONSTRUCTION ..........................................................................................................8 3. STRUCTURES................................................................................................................................9 3.1 EVAPORITE-RELATED FOLDS.................................................................................................................9 3.2 THRUST-RELATED FOLDS .....................................................................................................................9 3.3 TEAR FAULTS ..................................................................................................................................10 4. FERNSCHUB HYPOTHESIS...........................................................................................................11 4.1 MECHANICS ...................................................................................................................................11 4.1.1 Kinematics ...........................................................................................................................12 4.1.2 Critical taper........................................................................................................................13 4.2 LABORATORY EXPERIMENTS...............................................................................................................14 5. CONCLUSION.............................................................................................................................15 6. LITERATURE...............................................................................................................................16 3 The Geometry and Evolution of the Jura Mountains: Fernschub mechanics Tabea Kleineberg 319001 Abstract The Jura Mountains, representing the most external part of the Alpine chain at its North-western front, are divided into three parts, all featuring different structural styles, ranging from plain plateaux in the external and Tabular Jura to a well developed fold-train in the internal Jura. The Jura Mountains formed in the latest stage of the Alpine orogeny in Upper Miocene/ Lower Pliocene times and are closely linked to the Molasse Basin. Its basement is comprised of metamorphic rocks and is decoupled from the sediment cover by a basal décollement. Folding and thrusting is restricted to the sedimentary cover rocks, pointing to a thin-skinned fold-and-thrust tectonics, which require very low basal friction. When shortening in the subalpine Molasse reached the Jura, the décollement in the Triassic Evaporites sheared off into the foreland generating the thrusts and folds of the Jura Mountains. This process is called the Fernschub hypothesis by BUXTORF (1916) and it is, at the present day, the most broadly-acknowledged theory for the formation of the Jura Mountains. Its essence and mechanics will be discussed in this paper. 4 The Geometry and Evolution of the Jura Mountains: Fernschub mechanics Tabea Kleineberg 319001 1. GEological SEttIng The Jura Mountains are located in Central Europe, in the Northwest of Switzerland and in the East of France in front of the Western Alpine arc. Their length amounts to 370 km with a maximum width of 75 km (BECKER, 2000). Figure 1 shows the structural map of the Jura arc, with its division into the internal, external and Tabular Jura highlighted in different shades of grey. In the south, the Jura Mountains are linked with the Alpine front of the Prealps, however, in the northeast they are separated from the Alpine chain by the tertiary Molasse Basin which is up to 50 km wide close to the eastern termination of the Jura Mountains northwest of Zurich. The Molasse Basin correlates to an Oligo- Miocene foredeep, that developed in front of the Alpine orogen (SOMMARUGA, 1998). The crucial features along the western and northern border are the Tertiary rifts of the Bresse Depression and the Upper Rhine Graben (BECKER, 2000). The Rhine and Bresse Graben are associated with the Eocene and younger, West-European rift system. The Jura overthrusts the Bresse Graben in the west, and the Tabular Jura in the north (SOMMARUGA, 1998). Both rifts were active during the Eocene to Miocene, before Jura folding commenced (AFFOLTER ET AL., 2004). The remaining areas along the northern margin of the Jura folds belong to the Tabular Jura; the more or less unfolded, locally block faulted and non-decoupled sedimentary analogue of the folded Jura cover (BECKER, 2000). 001 A[ Sommaru`a:Marine and Petroleum Geolo`y 05 "0888# 000Ð023 FigurE 1: Structural skEtch of thE Jura MountaIns (SOMMARUGA, 1998). Fig[ 1[ Tectonic sketch of the Jura arc showing main structural units[ Legend] PHSPlateau de Haute!Sao¼ne^ ICIle Cre⇣mieu^ AMAvants! Monts^ FeFerrette^ ARAiguilles Rouges^ MBMont Blanc[ Modi_ed from Sommaruga "0884#[ Wegmann\ 0852^ Ziegler\ 0871# and\ on the other hand\ Jura and the Molasse Basin "Ziegler\ 0871^ Guellec et al[\ thin skinned thrusting and associated folding of the Jura 0889^ Gorin et al[\ 0882^ P_}ner\ 0883^ Signer + Gorin\ cover above a Triassic detachment horizon and dis! 0884^ P_}ner et al[\ 0886#[ For a more complete review placement over large horizontal distances pushed from on the evolution of the ideas on the formation of the Jura the Alps across the Molasse Basin "{Fernschub theory|# belt\ see Sommaruga "0886#[ "Boyer + Elliott\ 0871^ Buxtorf\ 0805^ Laubscher\ 0862b#[ Although balancing arguments clearly favor an allo! 1[ Geological setting chthonous interpretation\ seismic data as well as neo! tectonic arguments have recently been used to support The Jura is a small\ arcuate fold belt forming the fron! some thick!skinned basement involvement beneath the tal portion of the western Alpine arc "Fig[ 0#[ The Jura 5 The Geometry and Evolution of the Jura Mountains: Fernschub mechanics Tabea Kleineberg 319001 2. StratIgraphy and Evolution of thE Jura Mountains The Jura Mountains are a foreland fold-thrust belt, where the structural components involve a relatively thin sediment cover; approximately 2 km thick in the Internal Jura, deformed above a basal décollement within the Middle and Upper Triassic evaporites (Figure 3) (AFFOLTER ET AL., 2004). The Mesozoic and Cenozoic rocks are folded at variable degrees and detached from the gently 1-5° SE dipping pre-Triassic basement, illustrated by Figure 3 (SOMMARUGA, 1998 and BECKER, 2000). By contrast with the deformed Jura cover, the molasse fill of the foreland basin was left virtually un- deformed by Alpine deformations (Figure 3) (AFFOLTER ET AL., 2004). 2.1 BasemEnt The crystalline basement is composed of medium-to-high grade metamorphic and plutonic rocks, which were deformed during the Hercynian orogeny. The surface of the basement, including some Permo-Carboniferous troughs, is not strongly accentuated. Nowhere is it exposed in the Jura and Molasse Basin (BECKER, 2000). It is characterized by two major unconformities, one below the Carboniferous and the second below the Triassic (SOMMARUGA, 1998). Its tectonic style, the depth and geometry and its internal deformation are still uncertain (BURKHARD, 1990). Some moderate basement elevations, however, are proven along the Vuache fault system, the eastern border zone of the Bresse Depression, the southern rim of the Permo-Carboniferous Trough of northern Switzerland and in the Oyonnax region of the southern Jura Mountains. The depth of the basement varies from more than 7 km below sea level in front of the Aar massif to more than 4 km above sea level 20 km further to the southeast (Figure 3) (BECKER, 2000). 2.2 The sedimEnt cover The sediment cover of the Jura Mountains reaches maximum thicknesses of 1.5 km in the north, approximately 2 km in the centre and more than 3 km in the south (BECKER, 2000). It is separated from the basement by an evaporite layer (Figure 2 and 3, compare to 2.2.1). The Jura is divided into an external and an internal part, based on different tectonic styles (Figure 1). The external FigurE 2: StratIgraphy of thE Jura and adjacEnt Jura consists of flat areas, plateaux, separated from MolassE BasIn (modIfIEd aftEr SOMMARUGA, 1998). 6 The Geometry
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