New approach for the quantification of paleostress magnitudes: application to the Soultz vein system (Rhine graben, France)

André, Anne-Sylvie; Sausse, Judith; Lespinasse, Marc

doi:10.1016/s0040-1951(01)00103-2

Cited by 53 publications

(19 citation statements)

References 31 publications

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“…The Jolly and Sanderson (1997) method has been applied to multiples studies, especially to tectonics of hydrothermal and magmatic vein and dyke systems (André et al, 2001;McKeagney et al, 2004;Mazzarini and Isola, 2007; The stress analysis performed for the SE Sardinia dyke swarm yielded the orientation of the three principal stress axes from the resulting elongate cluster pattern of dyke wall poles (Fig. 9a), which indicates that the magmatic pressure was smaller than the magnitude of the intermediate stress (Pm < σ2).…”

Section: Regional Stress Field and Magmatic Pressurementioning

confidence: 99%

Structure and tectonic setting of the SE Sardinia mafic dyke swarm. Insights for the stress state during magma emplacement in the upper crust

Martínez-Poza

Druguet

2016

Journal of Geodynamics

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Section: Regional Stress Field and Magmatic Pressurementioning

confidence: 99%

Structure and tectonic setting of the SE Sardinia mafic dyke swarm. Insights for the stress state during magma emplacement in the upper crust

Martínez-Poza

Druguet

2016

Journal of Geodynamics

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“…13b). Use of the FIP orientation in structural geology has been developed in different studies for establishing relationships between tectonic events and fluid percolation (e.g., Pêcher et al 1985;Kowallis et al 1987;Laubach 1989;Cathelineau et al 1990;Lespinasse 1999;André et al 2001). The geometric parameters of the FIP sets were characterized by image analysis on oriented double-polished plates ( Fig.…”

Section: Geometry Of the Fluid Inclusion Planesmentioning

confidence: 99%

Internal vein texture and vein evolution of the epithermal Shila-Paula district, southern Peru

et al. 2006

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The epithermal Shila-Paula Au-Ag district is characterized by numerous veins hosted in Tertiary volcanic rocks of the Western Cordillera (southern Peru). Field studies of the ore bodies reveal a systematic association of a main E-W vein with secondary N55-60°W veins-two directions that are also reflected by the orientation of fluid-inclusion planes in quartz crystals of the host rock. In areas where this pattern is not recognized, such as the Apacheta sector, vein emplacement seems to have been guided by regional N40°E and N40°W fractures. Two main vein-filling stages are identified. stage 1 is a quartz-adulariapyrite-galena-sphalerite-chalcopyrite-electrum-Mn silicate-carbonate assemblage that fills the main E-W veins. stage 2, which contains most of the precious-metal mineralization, is divided into pre-bonanza and bonanza substages. The pre-bonanza substage consists of a quartz-adularia-carbonate assemblage that is observed within the secondary N45-60°W veins, in veinlets that cut the stage 1 assemblage, and in final open-space fillings. The two latter structures are finally filled by the bonanza substage characterized by a Fe-poor sphalerite-chalcopyrite-pyrite-galena-tennantite-tetrahedrite-polybasite-pearceite-electrum assemblage. The ore in the main veins is systematically brecciated, whereas the ore in the secondary veins and geodes is characteristic of open-space crystallization. Microthermometric measurements on sphalerite from both stages and on quartz and calcite from stage 2 indicate a salinity range of 0 to 15.5 wt% NaCl equivalent and homogenization temperatures bracketed between 200 and 330°C. Secondary CO 2 -, N 2 -and H 2 S-bearing fluid inclusions are also identified. The age of vein emplacement, based on 40 Ar/ 39Ar ages obtained on adularia of different veins, is estimated at around 11 Ma, with some overlap between adularia of stage 1 (11.4±0.4 Ma) and of stage 2 (10.8±0.3 Ma). A three-phase tectonic model has been constructed to explain the vein formation. Phase 1 corresponds to the assumed development of E-W sinistral shear zones and associated N60°W cleavages under the effects of a NE-SW shortening direction that is recognized at Andean scale. These structures contain the stage 1 ore assemblage that was brecciated during ongoing deformation. Phase 2 is a reactivation of earlier structures under a NW-SE shortening direction that allowed the reopening of the preexisting schistosity and the formation of scarce N50°E-striking S2-cleavage planes filled by the stage 2 pre-bonanza minerals. Phase 3 coincides with the bonanza ore emplacement in the secondary N45-60°W veins and also in open-space in the core of the main E-W veins. Our combined tectonic, textural, mineralogical, fluid-inclusion, and geochronological study presents a complete model of vein formation in which the reactivation of previously formed tectonic structures plays a significant role in ore formation.

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“…Using this assumption, and reversing it, Angelier (1975) proposed the 'reduced stress tensor' concept and stress ratio ½FZ ðs 2 K s 3 Þ=ðs 1 K s 3 Þ which describes the shape of the stress ellipsoid from which ratios of principal paleostress magnitudes can be calculated. However, determination of absolute magnitudes from natural examples of fault-slip data is possible to some extent (Bergerat, 1987;Angelier, 1989;André et al, 2001), but is generally very difficult, due to a number of unknowns related to the environmental conditions during faulting that cannot be obtained from fault-slip data alone. Therefore, the standard paleostress inversion techniques are used only for determining the orientations and relative magnitudes (stress ratios) of the regional principal stress axes (see Angelier, 1994 for a review of the method).…”

Section: Introductionmentioning

confidence: 99%

Kinematic development and paleostress analysis of the Denizli Basin (Western Turkey): implications of spatial variation of relative paleostress magnitudes and orientations

Kaymakçı

2006

Journal of Asian Earth Sciences

111

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New approach for the quantification of paleostress magnitudes: application to the Soultz vein system (Rhine graben, France)

Cited by 53 publications

References 31 publications

Structure and tectonic setting of the SE Sardinia mafic dyke swarm. Insights for the stress state during magma emplacement in the upper crust

Structure and tectonic setting of the SE Sardinia mafic dyke swarm. Insights for the stress state during magma emplacement in the upper crust

Internal vein texture and vein evolution of the epithermal Shila-Paula district, southern Peru

Kinematic development and paleostress analysis of the Denizli Basin (Western Turkey): implications of spatial variation of relative paleostress magnitudes and orientations

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