Determination of fluid-flow zones in a geothermal sandstone reservoir using thermal conductivity and temperature logs

Haffen, Sébastien; Géraud, Yves; Diraison, Marc; Dezayes, Chrystel

doi:10.1016/j.geothermics.2012.11.001

Cited by 46 publications

(34 citation statements)

References 29 publications

(25 reference statements)

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“…The evaluated porosity of the Buntsandstein is quite low (10% at the top of the formation and 20% for the Vosgian sandstones) (Vernoux et al 1995). Petrophysical studies of the core samples note the role of the matrix permeability, which controls the geothermal fluid circulation through these sandstones (Haffen et al 2013). The core sample exhibits a part of a fracture zone (1) and its damage zone (2).…”

Section: Geology Of the Sedimentary Covermentioning

confidence: 99%

How do permeable fractures in the Triassic sediments of Northern Alsace characterize the top of hydrothermal convective cells? Evidence from Soultz geothermal boreholes (France)

Vidal

Genter²,

Schmittbuhl

2015

Geotherm Energy

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Background: The thermal regime of the Upper Rhine Graben (URG) is characterized by a series of anomalies near Soultz-sous-Forêts (France), Rittershoffen (France), and Landau (Germany). These temperature anomalies are associated with groundwater circulation in fractures and faults distributed in the Cenozoic and Mesozoic sedimentary cover associated with and connected to fractures originating deep within the Paleozoic basement. The present study helps to understand the convective cell structure in order to optimize geothermal borehole trajectories. Methods: The work concentrated on a detailed interpretation of the geophysical and geological logs from Soultz geothermal wells mainly from the topographic surface to the Triassic formations, at between 800-and 1,400-m depth above the deep granitic basement.

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Section: Geology Of the Sedimentary Covermentioning

confidence: 99%

How do permeable fractures in the Triassic sediments of Northern Alsace characterize the top of hydrothermal convective cells? Evidence from Soultz geothermal boreholes (France)

Vidal

Genter²,

Schmittbuhl

2015

Geotherm Energy

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“…Few studies, especially laboratory studies that offer values of porosity and permeability, have targeted the overlying Permo-Triassic sedimentary units (e.g. Haffen et al 2013;Stober and Bucher 2015;Vidal et al 2015;Griffiths et al 2016). For example, Haffen et al (2013) estimated the permeability of the Buntsandstein sandstones of EPS-1 using a portable TinyPerm II permeameter and found that their permeability ranges from 10 −15 to 10 −13 m 2 .…”

Section: Introductionmentioning

confidence: 99%

“…Haffen et al 2013;Stober and Bucher 2015;Vidal et al 2015;Griffiths et al 2016). For example, Haffen et al (2013) estimated the permeability of the Buntsandstein sandstones of EPS-1 using a portable TinyPerm II permeameter and found that their permeability ranges from 10 −15 to 10 −13 m 2 . However, the laboratory measurements of Griffiths et al (2016) highlight that the permeability of Buntsandstein sandstones from EPS-1 can be lower than 10 −18 m 2 .…”

Section: Introductionmentioning

confidence: 99%

Microstructural and petrophysical properties of the Permo-Triassic sandstones (Buntsandstein) from the Soultz-sous-Forêts geothermal site (France)

et al. 2017

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Geothermal projects in the Upper Rhine Graben aim to harness thermal anomalies that have arisen due to hydrothermal circulation within the granitic basement and the overlying Permo-Triassic sedimentary units. We present here a systematic microstructural, mineralogical, and petrophysical characterisation of the lowermost unit of this Permo-Triassic sedimentary succession-the Buntsandstein-sampled from exploration well EPS-1 at the Soultz-sous-Forêts geothermal site (France). Twelve depths were sampled (from 1008 to 1414 m) and cylindrical cores were prepared perpendicular and parallel to bedding. These cores were described in terms of their microstructure, grain size and shape, specific surface area, pore size and pore throat size distribution, mineral content, porosity, P-wave velocity, and permeability. The Buntsandstein sandstones are predominantly feldspathic sandstones, often characterised by pores filled or partially filled (with clays (R3 illite-smectite), dolomite, siderite, and barite) as a consequence of diagenesis, tectonics, and the circulation of hydrothermal fluids. The porosity, dry P-wave velocity, and permeability of these sandstones vary from ~ 0.03 to 0.2, ~ 2.5 to 4.5 km s −1 , and ~ 10 −18 to 10 −13 m 2 , respectively. Our data show that P-wave velocity decreases and permeability increases as porosity increases. P-wave velocities are significantly higher when measured parallel to bedding (by about 10 to 25%), and that saturation with water increases P-wave velocity (by about 5 to 50%, depending on sample orientation). The pervasive pore-filling precipitation has significantly reduced the permeabilities of the Buntsandstein sandstones, which are orders of magnitude less permeable than similarly porous unaltered sandstone. We also find that their permeability can be up to an order of magnitude more permeable when measured parallel to bedding than perpendicular to bedding. Although Buntsandstein units with low matrix permeabilities (as low as ~ 10 −18 m 2 ) require macroscopic fractures to attain the high permeability required to sustain regional hydrothermal circulation, matrix permeability is important for units with low fracture densities and high matrix permeabilities. We anticipate that these data will aid future fluid flow modelling and seismic investigations at geothermal sites within the Upper Rhine Graben. Open Access© The Author(s) 2017. This article is distributed under the terms of the Creative Commons Attribution 4.0 International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.

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“…The sum of these two terms corresponds to the total source current density S j : (14) where u (in m· s −1 ) denotes the Darcy velocity, ˆV Q (in C· m −3 ) denotes the excess of electrical charge at saturation that is carried along with the flow of the pore water, σ denotes the (saturation-dependent) electrical conductivity of the porous material, and T C is the thermoelectric coupling coefficient defined below. For pH values between 5 and 8, Jardani et al [88] found that the ˆV Q is controlled by the permeability at saturation k (in m 2 ) and they developed the following empirical relationship [89]: 10 10 log 9.2 0.82log…”

Section: Self-potential Methodsmentioning

confidence: 99%

“…However, such models require the knowledge of the parameters governing groundwater flow (e.g., hydraulic conductivity and specific storage) and heat transport (e.g., thermal conductivity, volumetric heat capacity, flow rate). In situ tests, such as thermal response tests [12,13] or laboratory measurements [14] are sometimes possible, but the values obtained may deliver only well-centered information or may not always (if not at all) be representative of in situ conditions at a larger scale. Such data are often scarce if not missing and authors often have to rely on standard calculation charts, values found in the literature, or simply default values implemented in standard software (e.g., [15][16][17][18]).…”

Section: Introductionmentioning

confidence: 99%

Geophysical Methods for Monitoring Temperature Changes in Shallow Low Enthalpy Geothermal Systems

Hermans

Nguyen

Robert³

et al. 2014

Energies

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Low enthalpy geothermal systems exploited with ground source heat pumps or groundwater heat pumps present many advantages within the context of sustainable energy use. Designing, monitoring and controlling such systems requires the measurement of spatially distributed temperature fields and the knowledge of the parameters governing groundwater flow (permeability and specific storage) and heat transport (thermal conductivity and volumetric thermal capacity). Such data are often scarce or not available. In recent years, the ability of electrical resistivity tomography (ERT), self-potential method (SP) and distributed temperature sensing (DTS) to monitor spatially and temporally temperature changes in the subsurface has been investigated. We review the recent advances in using these three methods for this type of shallow applications. A special focus is made regarding the petrophysical relationships and on underlying assumptions generally needed for a quantitative interpretation of these geophysical data. We show that those geophysical methods are mature to be used within the context of temperature monitoring and that a combination of them may be the best choice regarding control and validation issues. OPEN ACCESSEnergies 2014, 7 5084

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Determination of fluid-flow zones in a geothermal sandstone reservoir using thermal conductivity and temperature logs

Cited by 46 publications

References 29 publications

How do permeable fractures in the Triassic sediments of Northern Alsace characterize the top of hydrothermal convective cells? Evidence from Soultz geothermal boreholes (France)

How do permeable fractures in the Triassic sediments of Northern Alsace characterize the top of hydrothermal convective cells? Evidence from Soultz geothermal boreholes (France)

Microstructural and petrophysical properties of the Permo-Triassic sandstones (Buntsandstein) from the Soultz-sous-Forêts geothermal site (France)

Geophysical Methods for Monitoring Temperature Changes in Shallow Low Enthalpy Geothermal Systems

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