- Open Access
Structure and nature of the Palaeozoic basement based on magnetic, gravimetric and seismic investigations in the central Upper Rhinegraben
© The Author(s) 2018
- Received: 17 April 2018
- Accepted: 5 July 2018
- Published: 18 July 2018
New and old magnetic and gravimetric data acquired in the frame of a geothermal project have been processed in N. Vosges and the adjacent Rhinegraben in order to identify the nature and tectonic framework of the graben basement and to select areas with a geothermal potential. In maps, the ENE–WSW striking units of N. Vosges can be followed beneath the sedimentary cover as far as the N35°-striking Upper Rhenish Shear Zone, which shifts these units towards NE. The magnetic basement S and SW of Strasbourg is interpreted as akin to the southern Champ du Feu Massif, consisting of I-type granitoids. Combined with new and old reflection seismic sections, the data show that the petrologic and tectonic contexts in the Illkirch-Grafenstaden area, where a geothermal project is planned, which is similar to the deep geothermal wells of Soultz and Rittershoffen 70 km to the north. The target zone is a N–S fault, partly normal and partly transpressive, which offsets the magnetic, I-type granitoids with high contents of uranium and thorium by about 800 m. Further exploitation of oil along the N–S footwall block attests to the geothermal potential of the area. The NW–SE transpressional regime favours the formation of cracks and increases the porosity and consequently fluid convection. The close borehole ESC-7 and modelling of the temperature distribution lead to expectations of a temperature of at least 150 °C on top of the granite and show that the temperature anomaly results from the heat-productive granitoids and from the blanket effect of the low thermal conductivity tertiary sediments.
- Palaeozoic basement
- Geothermal project
The second and most prominent heat contribution is attributed to the composition of the upper crust, in particular to the elevated concentration of heat-producing elements (HPE) in Palaeozoic granitoids (Vilà et al. 2010). Already in the 1970s, the magnetic surveys at the ground level of the graben between Strasbourg–Lahr and Wissembourg–Baden-Baden had shown a clear correlation of the magnetic anomalies with temperature anomalies in the Soultz and Eschau ridge areas (Edel et al. 1980). In the northern Vosges, Baden-Baden area, Odenwald and Spessart massifs, the geophysical investigations revealed that these strong magnetizations are related to arc magmatic granites, granodiorites, diorites and associated volcanites (Edel and Weber 1995) emplaced in the range 340–330 Ma above the southeast dipping subduction of the Rhenohercynian ocean (Krohe 1991; Oncken 1997; Altherr et al. 1999) (Figs. 1b, 4). The 500-km long, 80-km wide magnetic belt consists of a succession of narrower kilometric anomalies. Three of such magnetic belts cross the Palaeozoic northern Vosges and continue towards the NE beneath the sedimentary cover of the Rhinegraben. Baillieux et al. (2013) suggest that approximately 20% of the temperature anomalies in the Upper Rhinegraben could be attributed to radiogenic heat production in this type of crystalline basement.
The aim of this paper is to correlate specific areas with high geothermal potential with the geological and geophysical pattern of the Palaeozoic basement of the central Rhinegraben (Fig. 1b) based on (1) geothermal data from wells, (2) interpretations of old and new gravimetric and magnetic data and (3) old and new reflection seismic data. In particular, the link between magnetic anomalies and thermal anomalies is used to constrain the structure and nature of the Palaeozoic basement of the central Rhinegraben and to localize areas of high geothermal potential (Fig. 1b). Finally, this approach is used to evaluate the geothermal potential of the southern area of Strasbourg, where a deep geothermal project is planned.
Existing geological, geothermal and geophysical data for the northern Vosges and central Upper Rhinegraben
Previous geophysical investigations have shown that the magnetic anomalies, which strike NNE–WSW to NE–SW in the northern Vosges, continue in the same direction across the Rhinegraben towards the area of geothermal interest. Therefore, interpretations of geophysical data in terms of the petrology and structural pattern of the Rhinegraben basement require knowledge of the geological and geophysical characteristics of the northern Palaeozoic Vosges.
Geological units of the northern Vosges
The volcanic activity was manifested by the Middle Devonian and possibly older basalts and by acidic pyroclastic rocks that were formerly known as the “spilite-keratophyre association” of the Bruche valley. These rocks show bimodal tholeitic and calc-alkaline affinities (Ikenne and Baroz 1985). The southern part of the shallow and younger granites of the northern Champ du Feu Massif is overlain by a narrow belt of andesites, ignimbrites and tuffs and at its westernmost extremity by volcano-sedimentary rocks, forming the “Bande médiane”. In the western part of the belt, the calc-alkaline volcanic rocks of Visean age overlie terrains of supposed Devonian age, similar to those of the Bruche valley (Elsass and von Eller 2008) (Fig. 4). The last volcanic pulse occurred at the Carboniferous–Permian boundary approximately 297 Ma (Boutin et al. 1995). The rhyolitic magmatism of the Nideck–Donon, which was contemporaneous with the rhyolitic volcanism of the Black Forest and the Saar–Nahe, consists of rhyolites, ignimbrite and tuff flows and small granitic spots.
The plutonic complex of the Champ du Feu Massif crystallized in the Late Visean in a short time span between 336 and 326 Ma (Boutin et al. 1995; Hess et al. 1995; Altherr et al. 2000; Edel et al. 2013). The magmatic activity started with a succession of I-type granitoids forming two narrow dioritic belts striking NNE–SSW along the northern margin and in the central southern part of the pluton (the Neuntelstein diorites). The hornblende-bearing granodiorite of the Hohwald surrounding the Neuntelstein diorite belt was emplaced at a depth of approximately 10 km (Altherr et al. 2000) (Fig. 4). The magmatic activity further evolved to an S-type plutonism that is represented by the northern granitoid suite (Belmont, Waldersbach) with a concentric intrusive structure and a common granophyric microstructure and is emplaced at a shallow crustal level of 3–4 km depth (Altherr et al. 2000). The central elliptical part of the northern granite body (“Waldersbach” granite) is characterized by numerous xenoliths of volcanic-sedimentary rocks resulting from stopping of the Devonian–Carboniferous cover and by the intrusion of a more or less continuous belt of cogenetic hornblende-bearing microdiorite (Edel et al. 2013). The younger granitic stocks of Andlau and Natzwiller, respectively, intruded the schists of Steige and the Walderbach granite, whereas the ultrapotassic Kagenfels granite with its two E–W and N–S branches crosses the whole pluton.
The main tectonic feature is the E–W striking and subvertical Lalaye–Lubine fault zone that is commonly interpreted as being a dextral strike-slip (Fluck et al. 1989). The fault zone marks the boundary of the Saxothuringian Zone in the north and the Moldanubian Zone in the south (Kossmatt 1927; Edel and Schulmann 2009). South of the “Bande médiane”, an ENE–WSW and north dipping normal fault zone separates the shallow northern granites from the deeper southern granodiorites and diorites. North of the pluton, a nearly parallel normal fault zone, also north dipping, runs along the Bruche valley through Schirmeck (Fig. 4). Seismic and palaeomagnetic data show that the E–W to ENE–WSW faults were acting as normal faults during the NNW–SSE extension responsible for the SSE tilting of the plutonic units as well as that of the volcanic-sedimentary units of the Bruche valley that started approximately 330 Ma (Edel et al. 2013).
Existing geophysical data of northern Vosges and adjacent Rhinegraben
The available gravimetric data consist of a dense network of measurements carried out in the western Rhinegraben by CGG on behalf of the Mines de Potasse d’Alsace in the 1950s and plotted on hand-drawn Bouguer maps at a scale of 1/50,000. The maps were digitized and processed by Rotstein et al. (2006). The databases for the Vosges from the Bureau de Recherches Géologiques et Minières (BRGM) and the eastern Rhinegraben from the Bundesanstallt für Bodenforschung were compiled and added to the previous set. All of the results were presented in a global Bouguer map that included the Vosges, Rhinegraben and Black Forest (Rotstein et al. 2006).
The previous magnetic data concern only parts of the investigated area. They consist of (1) the aeromagnetic survey of NE France by the PREPA company, which was carried out in the early 1950s, digitized and plotted by Edel and Schulmann (2009), (2) the aeromagnetic map of Germany published by the BGR (1976) (Gabriel et al. 2011) and (3) the survey of the Rhinegraben at ground level by Edel et al. (1982) and Papillon (1995). The NNE strike of the gravimetric and magnetic anomalies suggests that rocks similar to those of the northern Vosges are expected in the adjacent Rhinegraben. Therefore, it is necessary to know the physical characteristics of the rocks in the Vosges. Subsequently, numerous available density, magnetic susceptibility and remanent magnetization measurements were summarized for this study in order to extrapolate gravimetric and magnetic anomalies from the Vosges massif to the Rhinegraben basement (Lauer and Taktak 1971; Gançarski 1977; Edel et al. 1982, 1986, 2013; Edel and Weber 1995; and unpublished data).
Among the numerous reflexion seismic profiles of the upper Rhinegraben, only those of the southern area of Strasbourg, where deep geothermal drillings are planned, are taken into account. There, four seismic 2D lines set up in 1985 for oil prospecting were reprocessed to obtain first order information at a quite low cost (Fig. 1).
Geothermal wells of the central Rhinegraben (Soultz and Rittershoffen)
The extensive geological, geophysical and deep drilling data collected in the Soultz and Rittershoffen geothermal wells have led to a better understanding of the deep-seated geothermal resources located at the interface between the sediments and the basement of northern Alsace (Baujard et al. 2017; Dezayes et al. 2010, Genter et al. 2010, Ledésert et al. 1999; Pribnow and Schellschmidt 2000; Sanjuan et al. 2016; Sausse et al. 2010; Vidal et al. 2016 , 2017).
From a structural point of view, the geothermal target of both wells corresponds to a local normal fault showing a significant apparent vertical offset. At Soultz, the natural fractures are mainly oriented N0°E, with nearly vertical dipping (Dezayes et al. 2010). At Rittershoffen, the fractures are also N–S striking (N10°E to N20°E) and dip westward in the reinjection well. In the production well, the main fracture orientation is N160°E to N180°E, dipping eastward or westward (Vidal et al. 2016).
All these wells were drilled down to the Triassic-sediments and/or the crystalline basement. Two main types of granites have been identified based on core samples collected in the Soultz wells: a biotite-rich monzogranite showing K-feldspar megacrysts emplaced approximately 330 Ma (Alexandrov et al. 2001) and a fine-grained two-mica granite. The Soultz site is located on the western margin of a magnetic body consisting of granitoids, whereas the Rittershoffen site is located more on its core (e.g. Baillieux et al. 2014).
From a thermic point of view, temperature measurements were performed in all wells of the Soultz and Rittershoffen sites. The temperature profiles in the Soultz wells can be divided into three sections with different geothermal gradients reflecting different heat transport processes (Fig. 3) (Genter et al. 2010). The upper section lies entirely in the sediments from the surface down to the top of the Muschelkalk formation and has a very high and linear gradient of approximately 90–100 °C/km, indicating a predominantly conductive heat transport (Maurer et al. 2018). The intermediate depth section is characterized by a very low geothermal gradient of approximately 5–10 °C/km, which suggests that heat transport is dominated by convection, probably within the fractured granite and in the Triassic sandstones. In the Soultz area, below 3.3 km, the geothermal gradient increases again to 30 °C/km and becomes linear with depth, indicating a return to a conduction-dominated heat flow regime (Genter et al. 2010) due to a weak connectivity of faults and fractures below 3.3 km depth. A temperature of 150 °C is reached at 3000 m in the granite. In the Rittershoffen wells, a temperature of 160° is already attained at 1600 m in the middle Triassic (Fig. 3). All the Soultz and Rittershoffen wells have demonstrated occurrences of geothermal fluids circulating within the natural fracture system developed within the deep granites. They correspond to geothermal brines characterized by a NaCl composition, high-salinity values ranging from 99 to 107 g/l and pH values close to 5 (Sanjuan et al. 2016). From a radiogenic point of view, the increase in gamma rays at the sedimentary/basement interface (from values lower than 100 gAPI to 250 gAPI at Soultz) can be interpreted as a result of precipitations of secondary minerals such as illite (clay mineral bearing potassium) from the geothermal brine into the hydrothermally altered and fractured granite in the upper part of the basement (Traineau et al. 1991).
New geophysical investigations
Two hundred fifty new gravimetric measurements were acquired in the frame of the Illkirch-Graffenstaden geothermal project (Fig. 1) in order to densify the network in areas of interest for geothermal projects. The compilation of old and new data resulted in a Bouguer map of the northern Vosges and adjacent Rhinegraben. This map is vertically derived in Fig. 5 in order to reduce the effect of the sedimentary cover, to constrain the boundaries of the gravimetric bodies and to facilitate the correlations with the magnetic map. The objective is to link the gravity anomalies with the density distribution of the outcropping basement available for rocks of the northern Vosges (Gançarski 1977; Edel and Weber 1995; and unpublished data) and to extrapolate the correlations to the Palaeozoic basement beneath the Rhinegraben sedimentary cover.
The further maps and interpretations addressed in this paper were achieved after removal of the International Geomagnetic Reference Field (IGRF) and anthropogenic anomalies. To optimize the interpretation, the magnetic anomalies have been reprocessed using several types of mathematical transformations. In the case of a symmetrical structure with a dominant induced magnetization, the associated magnetic anomaly is only symmetrical (pseudo-gravimetric) at the magnetic pole. The skewness or deformation of an anomaly is a function of the inclination of the magnetization, and in the case of a dominant induced magnetization, of the inclination of the magnetic field. In northern Alsace, this inclination is approximately 64°. To remove this effect, the anomalies have to be reduced to the pole. First and second vertical derivatives are used to delineate the boundaries of subvertical magnetic bodies (Fig. 6). Tilt is a transformation that also locates subvertical boundaries and faults, but in addition, it estimates the depths of the tops of the structures (Salem et al. 2007) (Fig. 7). The analytical signal and the square of the analytical signal delineate the fabric of the magnetic basement, but the intensity is also a function of the depth and the intensity of the magnetization.
Reprocessing of the four previous seismic sections was completed with a new survey and processing of vibroseismic reflections acquired within the “Illkirch-Erstein” licence in the southern suburbs of the Strasbourg area during the summer of 2015 (Fig. 1a). This 2D seismic survey was designed in order to qualify a potential deep fractured geothermal target (Richard et al. 2016). Obtaining a structural and hydrogeological model of this kind of deep fractured reservoir is a key point for a successful project (Dezayes et al. 2010). Therefore, geometry design and acquisition parameters have been designed to provide a suitable and valuable image of the sub-surface, particularly of faults (Appendix). The design of the new vibroseismic acquisition was focused on a specific area to ensure the trajectories of the future wells and to cross the previously identified targets. In the case of the Illkirch-Graffenstaden geothermal project, four new seismic profiles were implemented (Fig. 1a).
Gravity map of the northern Vosges and Rhinegraben
The positive Bouguer anomalies correlate with the high densities (2.9 > d > 2.75) of the Devono-Dinantian mafic volcanites of the Bruche valley and of the Early Palaeozoic schists of Steige and Villé (Gançarski 1977; Edel and Weber 1995). Devonian–Dinantian sedimentary and volcano-sedimentary rocks of the Bruche valley and the “Bande médiane”, gneisses of the Central Vosges, diorites (Neuntelstein) and granodiorites (Hohwald, Champ du Feu, Andlau) have intermediate densities. The negative anomalies are associated with low-density biotite granites and leucogranites of the northern pluton, with acidic volcanites and with Visean sediments (2.5 < d < 2.65).
The first vertical derivative of the Bouguer anomaly map shows a succession of N60° striking belts of anomalies (Fig. 5). In the south, the northern part of the Moldanubian central Vosges is characterized by low-to-intermediate anomalies associated with granites and gneisses. North of the Lalaye–Lubine fault zone, the high densities of the Villé and Steige schists are responsible for a positive anomaly that, east of a short gap attributed to the presence of granites, reappears in the southern part of the Erstein horst (Fig. 1) (Gançarski 1977; Edel and Weber 1995). Further north, the granitoid belts of the southern Champ du Feu pluton show intermediate densities and slightly weaker anomalies. East of these units, the intermediate anomalies of the northern Erstein horst may be due to the presence of similar rocks. This assumption is confirmed by the deep drilling MEI2, which has cored a monzonite similar to the Andlau granite. A sharp horizontal gradient that coincides with the “Bande médiane” separates the anomalies of the northern and southern Champ du Feu Massif. The low-density felsic granites in the north can be followed in the graben as far as the Strasbourg-Illkirch area, with an interruption south of Molsheim. Further north, the positive anomalies associated with the Devonian–Dinantian volcano-sedimentary units of the Bruche valley continue north of Molsheim towards the NE. North of these positive anomalies runs a belt of gravity lows that must be associated with light granites. The sole outcrop located on the axis of the negative anomalies is the small microgranitic dome of Blanc Rupt, which is located within the Nideck–Donon rhyolitic volcanites (Figs. 4, 5) The K–Ar age of 299 ± 9 Ma age of the microgranite granite is compatible with the 297 ± 9 Ma ages of the rhyolites and suggests that the northern low-density belt is mainly due to a late Carboniferous–early Permian magmatism (Boutin et al. 1995).
Magnetic maps of the Palaeozoic basement of the northern Vosges and Rhinegraben
The vertical derivative of the reduction to the pole shows three belts of magnetic anomalies striking N60° (Fig. 6). The southern one is located in the southern part of the Champ du Feu Massif and on the Meistratzheim–Eschau horsts. The second concerns the Bruche Valley, and further east the anomalies north of Molsheim. The third belt is located on a Wasselonne–Hoerdt line. Based on the transformed magnetic map and the derivatives, an attempt was made to delimit the magnetic basement structures and propose their lithological interpretation.
Interpretation and correlations of the gravimetric and magnetic maps
Lithology of the Rhinegraben basement
Within the graben, the derivative and tilt maps show two major belts of anomalies (Figs. 5, 6, 7, 8). The southern one, the Meistratzheim–Illkirch belt, is in the continuation of the southern Champ du Feu Massif, which consists mainly of I-type granitoids (Fig. 9). Gravimetric anomalies are intermediate to high, implying that similar rock types as diorites, granodiorites and metamorphic schists are expected. Remnants of volcano-sedimentary host rocks on top of the granitoids, as in the area of St-Nabor and the “Bande Médiane”, are not excluded. The depths of the magnetic bodies given by the tilt and the Vacquier methods range from 1.6 to 2.2 km.
The northern dense and highly magnetic belt includes the Devonian–Dinantian basin of the Bruche valley. The gravimetric and magnetic maps show a series of prominent positive anomalies, which in outcrops coincide with mafic Devonian–Dinantian volcanites. The anomaly highs associated with mafic rocks continue NE between Wasselonne and Molsheim (Figs. 5, 6). The dense but weakly magnetic rocks likely consist of Devonian–Visean volcano-sedimentary and sedimentary rocks similar to those of the Bruche valley. In the area of Mundolsheim, a gravimetric and magnetic low, which is at least partly due to the deepening of the basement (Fig. 1a), interrupts the volcano-sedimentary belt. Between Mundolsheim and Truchtersheim, the gravimetric low may indicate the presence of granite possibly covered by Permian layers. According to the very smooth bedding (Fig. 7), the low-to-intermediate magnetic anomalies have no sub-vertical contacts and are rather due to the presence of layered magnetic bodies consisting of volcanic or volcano-sedimentary strata overlying the granite. Unpublished modelling confirms this interpretation.
In the northeastern continuation of the poorly to moderately magnetic and low-density northern granites of the Champ du Feu Massif, the gravimetric and magnetic lows of the Mundolsheim–Strasbourg basin reveal a similar granitic basement possibly overlain by Permian sedimentary layers (Figs. 1, 9). Remnants of a “Bande médiane type” volcano-sedimentary cover on the felsic S-type granitoids, may also be expected. West of Strasbourg, the N60-65° striking granitic zone is crossed by a narrow, N30° oriented intermediate gravity high, which may be attributed to a horst effect (Fig. 1a) and/or to intermediate densities of non-magnetic Palaeozoic sediments. As confirmed by the tilt map, the very shallow depths of the anomalies of Strasbourg and its surroundings indicate anthropic origin.
Topography and tectonic framework of the basement of the central Rhinegraben
Due to its potential in oil and potash, the Rhinegraben subsurface was investigated using a dense network of seismic reflection profiles, which led to the production of Cenozoic and Mesozoic stratigraphic maps and of the faults associated with the graben formation. Although the Mesozoic/Palaeozoic boundary is often difficult to observe in the seismic sections, Ménard (1979) attempted to map the bottom of the Buntsandstein (Fig. 1a). The map shows two basins, the basin of Strasbourg–Mundolsheim in the north and the basin of Sélestat in the south. The Meistratzheim-Erstein and “Bois d’Illkirch-Graffenstaden-Eschau” horsts separate both basins.
The processed magnetic and gravimetric maps of this study are interpreted in terms of structural and lithological discontinuities of the pre-Permian basement. In addition to the global N60-65° trend of the Palaeozoic structures observed in the northern Vosges, the tectonic network of the basement beneath the Mesozoic–Cenozoic cover is dominated by N30° discontinuities, the effect of which is particularly visible on the truncation of the southern magnetic belt (Figs. 6, 7, 8, 9). The most important faults belong to the Upper-Rhine-Shear-Zone (URSZ), which shifts the Lalaye–Lubine fault zone by approximately 40 km northeastward, where it is relayed by the Baden-Baden fault zone (Edel and Fluck 1989; Edel et al. 2007). The sinistral URSZ that extends from the southeastern Vosges to the Mid-German Crystalline Rise was conjugated with the large-scale dextral faults of Bray and northern Bavaria (Edel and Weber 1995). The major N30° URSZ faults mark the eastern limit of the northern Vosges western Rhinegraben magnetic plutonic belt. The NE–SW fabric of the Andlau, Soultz-sous-Forêts and Baden-Baden granites implies that the granitoids were emplaced in the sinistral transcurrent regime active approximately 330 Ma (Edel et al. 2006). The plutonic complex is also affected by a series of sub-meridian faults. The best example illustrated as well by the magnetic as by gravimetric maps is the “Bois d’Illkirch-Graffenstaden-Eschau” N–S oriented horst (Figs. 8, 9). N–S faults are also present all along the western border of the Rhinegraben, from Molsheim to Dambach. The tectono-magmatic context of the southern plutonic belt looks very similar to that of the Odenwald massif, which belongs to the same Rhenohercynian magmatic arc that coincides with the Mid-German Crystalline Rise (Edel and Schulmann 2009). There, the I-type granitoids were emplaced in a WSW–ENE sinistral transtensional regime and affected in a late stage by the N–S normal Otzberg fault (Krohe 1991, 1992). To a lesser extent, NNW–SSE and NW–SE discontinuities conjugated with the ENE–WSW and NW–SE discontinuities are also present in the basement. Such discontinuities were active as dextral strike-slip faults in the area of the Champ du Feu Massif (Figs. 4, 9).
The target zone of the geothermal project
The characteristics of the potential deep-seated geothermal reservoir are discussed in light of the structural and petrological framework derived from the presented gravimetric and magnetic maps and of the information derived from the Soultz-sous-Forêts and Rittershoffen productive wells.
Structural context: the Eschau fault zone and the Bois d’Illkirch-Graffenstaden-Eschau horst: seismic interpretation
The thickness of the pre-Cenozoic layers in the area of the geothermal project remains relatively constant, implying that normal faulting was active in the Cenozoic. The TWT offset of the pre-Cenozoic reflectors is approximately 0.5 s. This corresponds to a 800–1000 m vertical offset of the Mesozoic layers and Palaeozoic basement along the fault zone. The onset of the N–S faulting likely occurred in the context of the N–S Late Eocene compression (Fig. 9, inset). Reactivation of the Variscan NE–SW sinistral strike-slip faults of the URSZ led to the formation of N–S oriented pull-apart basins (Villemin and Bergerat 1987; Schumacher 2002; Edel et al. 2007). The major activity of the Eschau fault zone is due to the E–W extension responsible for the Rhine–Rhone rifting that lasted during the whole Rupelian. The former transtensional N–S faults were active as normal faults up to the Chattian. This period is marked by a change of the stress regime. A NE–SW oriented compression phase occurred in western Europe and lasted into the middle Aquitanian (Villemin and Bergerat, 1987). In the Rhinegraben, it led to the formation of sedimentary depocentres parallel to the URSZ faults and to dextral transpressive activity along the N–S faults (Edel et al. 2006). The undulations in the upper Chattian Niederroedern layers located above the normal fault may reflect folding linked with the associated dextral strike slip (Figs. 9 inset, 10). Since the Middle Miocene, the principal orientation of stress has been oriented NW–SE, perpendicular to the Alpine front. This context favours NW–SE normal faulting and more often reactivates NNE–SSW sinistral basement faults, among others the URSZ faults (Edel et al. 2006). In the seismic sections, slight deformations of the Plio-Quaternary reflectors suggest a neo-tectonic activity above the fault zone (Fig. 10).
In most of the seismic sections, a relatively well-defined doublet of reflectors reveals a significant velocity contrast at the bottom of the Triassic sandstones (Buntsandstein) (Fig. 10).
Expected petrology and heat production
The Permian is absent in the Mei2 borehole, and the sandstones overly successively a granitic breccia and a biotite granite. In the northern Vosges, the Champ du Feu palaeosurface consists of granite and granodiorite often altered in arenas that constitute more or less thick, perched aquifers, some of which have been intensively investigated using geophysical methods (Sailhac et al. 2009). Such an altered and wet arena zone between the Buntsandstein and the granitoids is considered to be a good candidate for the deep seismic reflectors (Fig. 10).
In the northern Vosges, emplacement of the granitoids was responsible for contact metamorphism in the host rock. The volcanic, sedimentary or volcano-sedimentary rocks affected by contact metamorphism form a strong carapace that is extremely brittle. The presence of such rocks, akin to the development of faults and fractures during the tectonic evolution of the Rhinegraben is possible on top of the granitoids.
Petrophysical parameters used for modelling of the temperatures
Heat production (μW/m3)
Thermal conductivity (W/mK)
CF Nord granites
South CF granodiorites
W Black Forest granite
Felsique lower crust
The geothermal potential of the Eschau fault zone
The “Bois d’Illkirch-Graffenstaden-Maison-Blanche horst” was an oil reservoir exploited for several decades in a series of wells dispatched on a N–S line, parallel to the Eschau fault. The presence of oil reflects the high paleo temperatures associated with the respective oil generation window of the Illkirch-Graffenstaden-Eschau area, heat being necessary to oil production, in particular in the case of moderate depths of the mother rock.
By comparison with operational geothermal sites located in the Upper Rhinegraben, some favourable geological conditions for the Illkirch-Graffenstaden area can be anticipated. For instance, at Soultz-sous-Forêts and Rittershoffen, located approximately 50 km north of Strasbourg, several deep geothermal wells have been drilled in the basement at depths between 2.5 and 5 km (Fig. 1b). The experience acquired in those sites in terms of geothermal reservoirs is very useful to extrapolate to the Illkirch-Graffenstaden site before any drilling operations. Temperature and gamma ray profiles similar to those of the Rittershoffen and Soultz wells, which show a succession of conductive and convective sections and an increase in the natural radioactivity in the hydrothermally altered and fractured granite, are expected in Illkirch-Graffenstaden. This temperature increase is supposed to be due to accumulations of heat-producing elements (HPEs) related to secondary clay precipitations.
Like at Soultz and Rittershoffen, the productive wells of Illkirch-Graffenstaden will be drilled in submeridian faults. It is therefore anticipated that in the present stress field, the Eschau N–S faulted zone at the interface between the deepest sediments and the Palaeozoic crystalline basement could be characterized by a high concentration of closely spaced fractures acting as permeable drains. Just as at Soultz and Rittershoffen, where magnetic and heat-productive granites were drilled (Baillieux et al. 2014 and references therein), magnetic and heat-productive granodiorites of the southern champ du Feu type are expected.
In geophysical maps, the ENE–WSW striking units of the northern Vosges can be followed beneath the Mesozoic to Quaternary cover as far as the N35°-striking Upper Rhenish Shear Zone, which shifts these units towards the NE in the Baden-Baden area. From south to north, these units are the Early Palaeozoic Schist Zone (EPSZ), the Late Visean I-type Granite Zone (VIGZ), the Late Visean S-type Granite Zone (VSGZ), the Devonian–Dinantian volcanic-sedimentary Zone (DDVZ) and the Late Variscan Granite Zone (LVGZ) (Fig. 9). The granitoid belts are emplaced at higher levels and are younging from south to north. The magnetic basement south and south-west of Strasbourg is interpreted as akin to the southern Champ du Feu Massif, which consists of I-type granitoids. As these magmatic rocks intruded Early Palaeozoic schists and Devonian–Dinantian volcanic-sedimentary units, remnants of these host rocks on top of the pluton as the Bande Mediane and the St-Nabor units are not excluded.
The formation of oil within the sedimentary cover of the Soultz and Eschau areas is associated with high-temperature anomalies.
The submeridian Eschau fault consists of a several hundred-metres-wide fault zone, mainly active as normal faults in the Rupelian and transcurrent in the Priabonian, Chattian, Aquitanian and, in particular, recent times. The orientation and stress context are similar to those of the Soultz and Rittershoffen productive wells. The transpressional system favours the formation of cracks and increases the porosity and consequently fluid convection.
The basement consists of magnetic granitoids, as is the case at Soultz and Rittershoffen. In the northern Vosges, these magnetic granitoids are characterized by high contents of uranium and thorium and thus by heat production. The deeply rooted arc magmatic granitoids are also efficient thermal conductors of the deep-seated heat flow.
The close borehole ESC-7 and the modelled temperature distribution allow expectation of a temperature of a least 150 °C in the future geothermal doublet. Modelling of the temperature distribution based on a crustal section and appropriate physical parameters is also in favour of a minimum temperature of 150 °C on top of the granitic basement.
AG and VM are the leaders of the geothermal project. ED participated to the redaction of the paper. RH produced the temperature model. OL carried out the aeromagnetic survey. AR was in charge of the reflection seismics. JBE processed the gravimetric and magnetic data, interpreted the geophysical data, and edited a large part of the drafts. All authors read and approved the final manuscript.
This is a contribution of the EOST-IPGS (Ecole et Observatoire de Sciences de la Terre—Institut de Physique du Globe—Université de Strasbourg) and ESG (Electricité de Strasbourg—Géothermie) done in the framework of the EGS Alsace project and co-funded by Electricité de Strasbourg, the University of Strasbourg and ADEME (French Energy and Environnemental Agency). We thank Fonroche Géothermie for sharing aeromagnetic data and fruitful discussions before publication. The authors are grateful to GEIE EMC and ECOGI for sharing the Soultz and Rittershoffen well data, respectively. Dr. A.-S. Tabaud graciously provided the heat-production values of the northern Vosges granitoids. Prof. K. Schulmann kindly read the manuscript and made constructive comments and corrections. Two anonymous reviewers are thanked for their exhaustive reading and help in improving of the manuscript.
The authors declare that they have no competing interests.
We used published data or data acquired within the framework of this study.
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