Effect of Faulting on Fluid Flow in Porous Sandstones: Geometry and Spatial Distribution

Antonellini, Marco; Aydin, Atilla

doi:10.1306/8d2b1b60-171e-11d7-8645000102c1865d

Cited by 45 publications

(13 citation statements)

References 36 publications

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“…In addition, the interpretation that albite veins precipitated from hydrothermal fluids, produced by the mixing between metamorphic and magmatic fluids, reinforces the interpretation of an existing relay zone during this time, as these zones are preferential pathways for ascendant fluid flow, including hydrothermal, magmatic and metamorphic fluids, and therefore for cement precipitation (Antonellini and Aydin, 1995;Rotevatn et al, 2007;Fossen and Rotevatn, 2016). Moreover, because of the low porosity and permeability of the phyllites, the hydrothermal upflow was especially focused through the relay fractures that increased the permeability.…”

Section: Structural Evolution and Fracture Development Of The Turó Desupporting

confidence: 55%

Fluid composition changes in crystalline basement rocks from ductile to brittle regimes

Cantarero

Alías

Cruset

et al. 2018

Global and Planetary Change

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The relationships between deformation and fluid flow have been investigated in the Paleozoic basement of an isolated horst of the Catalan Coastal Ranges. A structural, petrological and geochemical study has been performed in a complex fracture network that resulted from a long-lived tectonic history (from Carboniferous to Miocene). Nine fracture types, developed from a ductile regime in the greenschist facies to a shallow brittle regime, have been characterized in order to establish P, T and fluid compositions during the evolution of the horst. Syn-cleavage and late-cleavage quartz veins (qtz1-chl1±mu and late qtz2-chl2-dol1) formed during the Hercynian ductile deformation. These minerals precipitated from metamorphic fluids, possibly evolved from seawater, at temperatures between 240 and 340ºC. En-echelon albite vein arrays (ab-qtz3-chl3±ti-an) and NE-SW normal faults generating breccias mark the change from ductile to brittle, from compression to extension and from a closed to an open hydrologic regime. This paragenesis precipitated from the mixing of metamorphic and magmatic fluids at temperatures 2 between 180 and 290ºC during the early Permian extension. Dolomite veins (dol2-chl4-qtz4), precipitated at 210-280ºC from the mixing of previous fluids with hypersaline oxidizing external brines, possibly during the late stage of the early Permian extension. Reverse faults and calcite veins (Cc1-ba) formed either during the Paleogene compression or during the Langhian to early Serravallian minor compression. Calcite and barite precipitated from meteoric or marine waters in an open hydrological system at temperatures below 50ºC. The Miocene extension is represented by NE-SW normal faults with fault gouges and NNW-SSE normal faults cemented by calcite 2 that precipitated at temperatures below 50ºC from meteoric fluids in an open basin-scale hydrological system. The studied horst was part of a relay zone between two segments of the NNW-SE Llobregat fault during the early Permian, explaining the high fracture density and the fast upflowing of hydrothermal fluids at that time, thus controlling the development of albite veins exclusively in this area.

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Section: Structural Evolution and Fracture Development Of The Turó Desupporting

confidence: 55%

Fluid composition changes in crystalline basement rocks from ductile to brittle regimes

Cantarero

Alías

Cruset

et al. 2018

Global and Planetary Change

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“…The overall global structure of a fault zone includes a fault core surrounded by damage zone domains (Chester and Logan, 1986;Antonellini and Aydin, 1994;Caine et al, 1996Caine et al, , 2010Heynekamp et al, 1999;Jourde et al, 2002;Fossen et al, 2005;Faulkner et al, 2010;Bense et al, 2013). The damage zone has characteristics that vary according to the rock type: 1) For brittle consolidated rocks, in the model of Caine et al (1996) the damage zone is defined as an increased fracture density and contains minor faults compared to the protolith.…”

Section: Introductionmentioning

confidence: 99%

“…The damage zone has characteristics that vary according to the rock type: 1) For brittle consolidated rocks, in the model of Caine et al (1996) the damage zone is defined as an increased fracture density and contains minor faults compared to the protolith. 2) For porous sandstones, models of the damage zone from Heynekamp et al, (1999) modified by Loveless et al, (2011), include minor faults and deformation bands (Antonellini and Aydin, 1994;Flodin et al, These processes interact with one another, because of their potential co-eval formation (Clauer et al, 2008;Worden and Morad, 2009).They have an impact on the pore network and reservoir quality of sandstones, though their quantification is rarely determined (Bjorlykke and Egeberg, 1993;Bjorkum, 1996;Worden and Burley, 2003;Eichhubl et al, 2009;Henares et al, 2016).…”

Section: Introductionmentioning

confidence: 99%

Pore network properties of sandstones in a fault damage zone

Bossennec

Géraud

Moretti³

et al. 2018

Journal of Structural Geology

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The understanding of fluid flow in faulted sandstones is based on a wide range of techniques. These depend on the multi-method determination of petrological and structural features, porous network properties and both spatial and temporal variations and interactions of these features. The question of the multi-parameter analysis on fluid flow controlling properties is addressed for an outcrop damage zone in the hanging wall of a normal fault zone on the western border of the Upper Rhine Graben, affecting the Buntsandstein Group (Early Triassic). Diagenetic processes may alter the original pore type and geometry in fractured and faulted sandstones. Therefore, these may control the ultimate porosity and permeability of the damage zone. The classical model of evolution of hydraulic properties with distance from the major fault core is nuanced here. The hydraulic behavior of the rock media is better described by a pluriscale model including: 1) The grain scale, where the hydraulic properties are controlled by sedimentary features, the distance from the fracture, and the impact of diagenetic processes. These result in the ultimate porous network characteristics observed. 2) A larger scale, where the structural position and characteristics (density, connectivity) of the fracture corridors are strongly correlated with both geo-mechanical and hydraulic properties within the damage zone.

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“…The key architectural elements are the fault core and bounding damage zone ( Figure 2), both of which differ structurally and mechanically from the undeformed protolith (Caine et al 1996;Knott et al 1996;Kim et al 2004). Grain-size reduction and/or mineral precipitation in the fault core generally yields lower permeability than undeformed protolith (Antonellini and Aydin 1994;Evans et al 1997 permeability relative to both the core and the undeformed protolith, and the juxtaposition of these elements ( Figure 2) creates major permeability contrasts within the fault zone (Goddard and Evans 1995;Caine et al 1996;Wibberley and Shimamoto 2002). Damage zone permeability can be 2 to 3 orders of magnitude greater than the permeability of fractured protolith and four to six orders of magnitude greater than the fault core permeability (Caine et al 1996).…”

Section: Introductionmentioning

confidence: 99%

The Role of Fault‐Zone Architectural Elements on Pore Pressure Propagation and Induced Seismicity

Ortiz¹,

Person

Mozley

et al. 2018

Groundwater

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We used hydrogeologic models to assess how fault-zone properties promote or inhibit the downward propagation of fluid overpressures from a basal reservoir injection well (150 m from fault zone, Q = 5000 m /day) into the underlying crystalline basement rocks. We varied the permeability of the fault-zone architectural components and a crystalline basement weathered layer as part of a numerical sensitivity study. Realistic conduit-barrier style fault zones effectively transmit elevated pore pressures associated with 4 years of continuous injection to depths of approximately 2.5 km within the crystalline basement while compartmentalizing fluid flow within the injection reservoir. The presence of a laterally continuous, relatively low-permeability altered/weathered basement horizon (k = 0.1 × k ) can limit the penetration depth of the pressure front to approximately 500 m. On the other hand, the presence of a discontinuous altered/weathered horizon that partially confines the injection reservoir without blocking the fault fluid conduit promotes downward propagation of pressures. Permeability enhancement via hydromechanical failure was found to increase the depth of early-time pressure front migration by a factor of 1.3 to 1.85. Dynamic permeability models may help explain seismicity at depths of greater than 10 km such as is observed within the Permian Basin, NM.

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Effect of Faulting on Fluid Flow in Porous Sandstones: Geometry and Spatial Distribution

Cited by 45 publications

References 36 publications

Fluid composition changes in crystalline basement rocks from ductile to brittle regimes

Fluid composition changes in crystalline basement rocks from ductile to brittle regimes

Pore network properties of sandstones in a fault damage zone

The Role of Fault‐Zone Architectural Elements on Pore Pressure Propagation and Induced Seismicity

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