Evolution of diagenetic conditions and burial history in Buntsandstein Gp. fractured sandstones (Upper Rhine Graben) from in-situ δ¹⁸O of quartz and ⁴⁰Ar/³⁹Ar geochronology of K-feldspar overgrowths

Abstract

In-situ δ¹⁸O measured in the quartz overgrowths help identify temperature and fluid origin variations responsible for cementation of the pore network (matrix and fracture) in the Buntsandstein Gp. sandstone reservoirs within the Upper Rhine Graben. The overgrowths record two types of the evolution of δ¹⁸O: 1) a monotonous decrease of the δ¹⁸O_overgrowth interpreted as linked to an increasing burial temperature and 2) random fluctuations, interpreted as pointing out the injection of allochthonous fluids in faulted areas, on the cementation processes of the pore network (both intergranular and fracture planes). Fluids causing the quartz cementation are either autochthonous buffered in ¹⁸O from clay illitisation; or allochthonous fluids of meteoric origin with δ¹⁸O below − 5%. These allochthonous fluids are in thermal disequilibrium with the host sandstone. The measured signal of δ¹⁸O_overgrowth measured from samples and calculated curves testing hypothetic δ¹⁸O_fluid are compared to T–t evolution during burial. This modelling proposes the initiation of quartz cementation during the Jurassic and is validated by the in-situ ⁴⁰Ar/³⁹Ar dating results obtained on the feldspar overgrowths predating quartz overgrowths. A similar diagenetic history is recorded on the graben shoulders and in the buried parts of the basin. Here, the beginning of the pore network cementation predates the structuration in blocks of the basin before the Cenozoic graben opening.

Introduction

Cementation is a crucial feature of sandstone reservoir quality and was the topic of numerous studies (Houseknecht 1984; McBride 1989; Lundegard 1992; Bjørlykke and Egeberg 1993) and is still the focus of recent studies (Fischer et al. 2013; Bjørlykke 2014; El-Khatri et al. 2015; Henares et al. 2016; Yuan et al. 2017; Schmidt et al. 2020). Quartz overgrowths can be important authigenic minerals in deeply buried sandstones. Thus, triggered by fluid flow and compaction, the development of quartz overgrowths may reduce the initial porosity and impact permeability (Worden and Morad 2000; Götte et al. 2013; Therkelsen 2016). It is crucial to understand the pathways, timing, and origin(s) of the fluid(s) responsible for quartz cementation to improve diagenetic heterogeneity prediction in reservoirs. In-situ stable oxygen isotope geochemistry analysis can help to improve the understanding of the origin of clastic sediments and their post-depositional history by supplying information on (1) composition of the detrital grains; (2) composition of quartz cement; and (3) composition of diagenetic fluids and temperature of cementation (Götze et al. 2012; Hyodo et al. 2014; Pollington et al. 2011).

The nature and temperature of fluids flowing in faults are strongly impacting the properties and mineralogy of rock volumes in the vicinity of faults, especially the permeability distribution in petroleum and geothermal reservoirs, which may additionally result in reservoir compartmentalisation (Labaume and Moretti 2001; Brockamp and Clauer 2005; Faulkner et al. 2010; Aretz et al. 2015; Navelot et al. 2018).

The reconstruction of the paleo-water composition and the flow conditions inside the formation in this context is a challenge due to the uncertainties on the parameters which can control the onset of quartz cementation in sandstones:

• (1) Fluid isotope composition (Valley and Graham 1996; Pollington et al. 2011; Yuan et al. 2017).

• (2) Temperature (Walderhaug 1994; Marfil et al. 1996; Worden and Morad 2000; Sharp et al. 2016).

• (3) Local fluid–rock interactions (including the presence of clay mineral grain coatings) (Bjørkum et al. 1998; Fisher et al. 1999; El-Khatri et al. 2015; Zhu et al. 2015).

K-feldspar overgrowths are also common in sandstones (Sizun 1995; Worden and Burley 2003). They usually have a slightly different chemical composition than the detrital feldspars, leading to differential chemical reactivity and stability during diagenesis (Sizun 1995; Mark et al. 2006; Milovský et al. 2012). Diagenetic K-feldspars are not limited to early diagenesis and shallow burial depth (Mark et al. 2005), and their dating can improve the understanding of the burial history (Mark et al. 2006).

The Buntsandstein Gp. sandstones are one of the primary targets for geothermal and hydrocarbon resource production in the Upper Rhine Graben due to their porosity (both fracture and intergranular porosity) and relatively high permeability (Haffen et al. 2015; Böcker et al. 2016; Kushnir et al. 2018; Vidal and Genter 2018). As the flow pathways in these sandstones are composed of 1) large fault pathways and 2) intergranular pore and fracture network, it is essential to have an integrated overview of the conditions of formation and distribution of quartz overgrowths at the basin scale. This approach must consider the plumbing complexity leading to the present-day situation and should be associated with various fluid-flow phases.

In this study, we focus on the nature of fluids and their temperature. The other parameters, i.e., the initial porosity and the surface available for cementation, are not the focus of this study. The effect of pressure on quartz cementation has been investigated by several authors and is considered of secondary importance (Bjørlykke and Egeberg 1993; Worden and Morad 2000).

Burial temperatures reached by the sandstones can be estimated to assess a credible fluid source. The chosen strategy consists of the modelling of several hypotheses on the fluid isotopic signature and temperature regime. This strategy was chosen as the tool of fluid inclusions is, in this case, not available. Fluid inclusions in the studied quartz overgrowth are very sparse and too small to perform thermometry and further fluid analysis.

K–Ar ages on authigenic illite within the Buntsandstein Gp. sandstones reveal illitisation events in the Late Jurassic, recorded in several locations (Meyer et al. 2000; Brockamp and Clauer 2005; Blaise et al. 2016). Some of these illitisation events with varying isotopic composition are reported as related to hydrothermal fluid flow (with a fluid temperature above 200 °C) within fault zones and others related to burial diagenesis. The remaining questions are the timing of these phases, how fluid flows within the sandstones, and how it interacts and affects reservoir cementation and compartmentalisation. Here, these aspects are considered, as samples located in the vicinity of major faults were investigated and compared with other samples located away from large fault zones. Burial T–t models propose explanations for the isotopic signatures of diagenetic overgrowths.

We aim to address three research objectives: (1) the provenance of detrital grains; (2) the timing of diagenetic reactions; and (3) the provenance, nature, and flow pathways within the Buntsandstein Gp. sandstones. After focusing on the geological complexity to define the burial model, we present the oxygen isotope composition of quartz grains and overgrowths and ⁴⁰Ar/³⁹Ar geochronology on detrital K-feldspar grains and overgrowths. The results are integrated into the pragenetic sequence to discuss the fluid origin, temperature, and timing of diagenetic processes. Subsequently, we propose a novel interpretation of the Buntsandstein Gp. fluid flow history, integrating the key role of plumbing, i.e., major faults and fracture and pore network features.

Geological background

The Upper Rhine Graben (URG) is a widely studied example of a syn-orogenic continental foreland rifting (Illies 1972; Bergerat 1987; Ziegler 1992; Merle and Michon 2001; Edel et al. 2007; Ford et al. 2007; Bourgeois et al. 2007). This extensional basin was formed by complex, large-scale structural features, which strongly affected the organisation of syn-rift sedimentary systems (Schumacher 2002; Derer et al. 2005; Roussé 2006).

Structural features

The URG belongs to the central part of the European Cenozoic Rift System (ECRS), extending from the North Sea to the Mediterranean, over more than 1000 km (Illies 1972; Ziegler 1992; Ziegler et al. 1995). Today, the Vosges and Black Forest Massifs constitute the western and eastern shoulders of the rift, respectively. The URG is bordered in its northern part by the Rhenish Massif and in the South by the Jura Massif (Fig. 1A). This basin is oriented NNE/SSW and segmented into several sub-basins (Schumacher 2002). Transfer zones inherited from preexisting variscan lineaments separate these sub-basins (Derer et al. 2005).

Fig. 1

modified from Sokol et al. (2013)) of the western border of the URG with the location of Cleebourg and Soultz sites (see Fig. 1 a) E Schematic cross section (modified from Sokol et al. (2013)) of the western border of the URG with location of Roemerberg wells

Geological context and sampling localities: A Schematic geological map of the URG after Bossennec et al. (2018) and Eisbacher and Fielitz (2010) with sampled localities in pink. Major Variscan and Cenozoic faults are represented after Schumacher (2002). BL: Badenweiler–Lenzkirch fault system, LB: Lalaye–Lubine–Baden–Baden fault system, SHB: South Hunsrück–Taunus Border fault system. B Local geological map of Marlenheim outcrop. C Local geological map of Reichenberg outcrop. D Schematic cross section (

Pre-rift tectono-sedimentary history

The pre-rift tectono-sedimentary context is complex (Fig. 2A). The targeted sandstones belong to the Buntsandstein Gp. dates from the Late Permian to Early Triassic (Induan-Olenekian) (Bourquin et al. 2006, 2007). The Buntsandstein Gp. sandstones were deposited in a fluvial and playa-lake system, which was covering the Variscan basement and Permo-Carboniferous NE striking basins at the southern border of the Western Germany sag basin (Bourquin et al. 2006, 2009; Soyk 2015). The area of the future URG was subsiding from the Triassic to the Jurassic (Ziegler 1990, 1992). This phase was followed by an uplift-erosion phase from the Cretaceous to Early Eocene, which resulted in a SE dip of the Mesozoic series. The main uplift area was probably formed NW–NNW from the central URG and associated with synchronous volcanism (75–50 Ma) in the Rhenish Massif. This uplift was also contemporaneous to a long-wavelength folding episode of the lithosphere, related to the Alpine Tethys' geodynamical development (Ziegler et al. 2007; Bourgeois et al. 2007). Some studies suggest fault reactivations before the main Late Eocene subsidence episode, in association with volcanism on the northwestern margin of the Upper Rhine Graben, with the example of the Kisselwörth diatreme, which was ⁴⁰Ar/³⁹Ar dated to 55.8 ± 0.2 Ma (Lutz et al. 2013).

Fig. 2

A Chronological chart, modified after Böcker and Littke (2015) and Bossennec et al. (2018), placed in the frame of major geodynamical episodes. Paleostress orientations are represented in black for σ1, grey for σ2, and white for σ3; regional stress fields and geodynamical context (Schumacher 2002; Blaise et al. 2016). The hydrothermal activity is represented qualitatively (Walter et al. 2018). B Hydrothermal veins paragenesis synthesis (Pfaff et al. 2010; Staude et al. 2012; Bons et al. 2014; Burisch et al. 2017a, b). C Paragenetic sequence in Buntsandstein Gp. Sandstones (Soyk 2015)

Syn-rift tectono-sedimentary history

The opening and development of the URG were contemporaneous with the collisional phases of the Pyrenean and Alpine orogeny (Schumacher 2002; Dèzes et al. 2004) (Fig. 2A).

The first stages of rifting started during a phase of regional uplift and volcanism during the Middle Eocene NW from the central URG (Volcanism in the Hocheifel at approx. 44–35 Ma (Lutz et al. 2013)), sedimentation started in mini basins with an NE–SW orientation. These early rift basins, dated from the Late Ypresian–Lutetian, were filled with siliciclastic detrital products of the erosion of the uplifted graben shoulders evolving laterally to clay–limestones layers toward depocenters. (Roussé 2006; Eisbacher and Fielitz 2010).

From 46 to 37 Ma, with the increase of the basins sizes, sedimentation evolved into marly-bituminous clays, coals, and freshwaters limestones, characterising shallow lacustrine environments under a humid and warm climate (Sissingh 1998; Böcker et al. 2016). An increase in subsidence characterised the Late Eocene period. Marly and calcareous deposits belonging to the 'Grüne Mergel' member recorded first marine ingressions from the South (Meulenkamp and Sissingh 2003; Châteauneuf and Ménillet 2014). During the Oligocene, the area entered thermal subsidence, associated with a regional WNW–ESE extensional regime (Schumacher 2002; Berger et al. 2005). The whole basin was flooded by marine ingressions several times during the Rupelian, and the deposition of clayey organic-rich marls occurred even near the current graben margins. In the late Oligocene and Miocene, the regional stress regime changed to a transtensive sinistral shear. A new depocenter was established in the northern part of the URG, the Heidelberg–Mannheim Graben (Schumacher 2002). This new stress regime also developed a gradual uplift of the southern URG (Timar-Geng et al. 2006). A lithosphere folding event which began during the Burdigalian, at 17 Ma, caused the uplift of the southern URG (Dèzes et al. 2004; Ziegler et al. 2007; Bourgeois et al. 2007; Reicherter et al. 2008) and reactivated basement faults striking NE (Rotstein et al. 2005, 2006; Edel et al. 2007). A regional erosion of late Oligocene sediments occurred during the Middle Miocene uplift, giving the URG a geometry close to the current one. The northern URG underwent the third phase of subsidence from the Pliocene to Quaternary (Larroque and Laurent 1988; Schumacher 2002; Dèzes et al. 2004; Cloetingh et al. 2005). The lithospheric folding might also have played a role in the current geometry of the URG through crustal subsidence in the northern URG (Dèzes et al. 2004; Cloetingh et al. 2005, 2006).

Fluid history

During its complex burial history, Buntsandstein Gp. sandstones were exposed to varying temperature and fluids (regional hydrothermal activity, Fig. 2B), resulting in a multi-stage paragenetic sequence (Fig. 2C), strongly dependent on fault activity (Clauer et al. 2008; Dresmann et al. 2010; Blaise et al. 2016; Bossennec et al. 2018). The paragenetic sequence of the targeted sandstones is characterised by the first phase of diagenetic clay mineral grain coating, followed by the first generation of K-feldspar overgrowths. Quartz cementation is the third stage of the paragenetic sequence and is followed by an extensive illitisation, already documented within Lower Triassic sandstones in the Paris Basin (Blaise et al. 2016). In the meantime, several hydrothermal events are recorded regionally (Fig. 2B), with several pulses recorded within the underlying basement and with fault zones affecting the sedimentary deposits since the Triassic (Boiron et al. 2011; Loges et al. 2012; Walter et al. 2016, 2019; Dezayes and Lerouge 2019). Quartz, siderite, and barite mineralise in the fracture network linked to fault systems that were active during rift opening. This facture diagenesis suggests external fluid flow through the fracture network during Cenozoic hydrothermal events relative to the rift opening.

The focus of this study is to derive possible fluid sources affecting Buntsandstein Gp. sandstone diagenesis, their likely migration pathways and timing (Fig. 2C).

Materials and methods

Sampling

The samples were retrieved from different URG locations (Figs. 1, 3 and Table 1). All belong to the Buntsandstein Gp. sandstones but have varying burial histories. Samples from the URG shoulders (Marlenheim, Cleebourg, Reichenberg) were at their maximum burial depth during the Cretaceous. In contrast, samples currently located in deep-seated reservoirs reached their maximum burial during the Cenozoic. Samples divide into two categories: Category F) for samples having a fracture intensity (> 4 fractures. m⁻¹) from within a fault zone; Category C) for "clean" samples with an undisturbed intergranular space which do not present deformation-related microstructural features. For quartz overgrowths, samples X009 from Marlenheim (Fig. 1B) and B002 from Reichenberg (Fig. 1C) are selected from outcrops located on eastward tilted blocks on the footwall of the major fault system bordering the western side of the URG. The fault in Reichenberg vicinity strikes N020°E. Sample X024 (Marlenheim) is located on the tilted blocks footwall, in a fracture cluster sub-parallel to the major fault striking N035°E Sample K466 from Cleebourg (Fig. 1D) is located in the footwall damage zone of a fault within the western graben shoulders major fault system. The Cleebourg fault strikes N010°E. Sample EPS11360 is from the EPS1 borehole, drilled in the Soultz horst (Fig. 1D). Samples A-2783, B-2882, D-2537, E-2671, F-3225 belong to wells from the Central URG (Roemerberg, Fig. 1E). The wells are located on the nose of tilted blocks delimited to the west by a N020°E striking fault. Samples analysed for K–Ar overgrowths were selected within the same localities (Table 1, Fig. 4).

Fig. 3

Examples of profile measurements (red arrows) performed within detrital (DQ) and quartz overgrowths (QO) (SEM–CL)

Table 1 Sample description, with location, host-rock, category, type of analyses performed, and burial sequence type

Petrographic characterisation

Standard 30 µm polished thin sections and double side polished thick sections for Ar/Ar analyses were prepared for petrographic and microstructural analysis. Broad imaging of these sections was performed with a Tescan Vega3 Scanning Electron Microscope (SEM). Analysis conditions were set to a beam intensity of 8–10 nA and a voltage of 15 kV. Cathodoluminescence (CL) allows easy characterisation of quartz and feldspars overgrowths generations, grain deformation, and recrystallisation. Thus, authigenic phases identification was executed through SEM imaging, backscattered electron (BSE), and cathode-luminescence (CL) observations performed on a hot cathode on Tescan VEGA3 SEM device with a current intensity of 15–17nA and a voltage of 15 kV.

Isotope analysis

In-situ oxygen isotope analysis

The oxygen isotopic ratios of quartz overgrowths and detrital grains were determined using a Cameca IMS 1270 ion microprobe at CRPG laboratory (Nancy, France). Analyses were acquired on a total of 634 points on 10 samples. The Cs⁺ primary beam was settled with a spot diameter of 15–20 µm, an intensity of 8–10 nA, and an acceleration voltage of 10 kV. ¹⁶O⁻ and ¹⁸O⁻ secondary anions were multi-collected in two Faraday cups.

Spots were acquired following profiles in overgrowths, from the border with the detrital grain to the cement outer border, as presented in Fig. 4.

Fig. 4

Macroscopic and SEM–BSE photographs of sample categories: A D-2537: Example of fractured core-sample (category F). B B-2882: Example of non-fractured core sample (category C). C Sample X024: Example of fractured outcrop sample (category F). D Sample K500: Example of non-fractured outcrop sample (category C)

Ratios were calculated using the conventional notation presented in Eq. (1) and expressed in %V-SMOW for both fluids and quartz overgrowths:

$$\delta ^{{18}} O_{{spot}} = ~\left( {\frac{{~^{{18}} O/~^{{16}} O~_{{spot}} }}{{~^{{18}} O/~^{{16}} O_{{SMOW}} }}~ - ~1} \right) \times 1000$$

(1)

The quartz CRPG internal standard was measured in between each sample, and the error on measurements was corrected with a time-dependent linear trend. The precision of measurements is ± 0.2 %.

⁴⁰Ar/³⁹Ar geochronology

Argon isotope analysis with UV laser ablation (Kelley et al. 1994) was performed at the ⁴⁰Ar/³⁹Ar geochronology laboratory of the Institute of Earth and Environmental Science, at the University of Potsdam (Germany) in 2018. Samples providing the largest feldspar overgrowths were selected from 4 locations (Cleebourg, Soultz, Roemerberg, and Marlenheim). Reichenberg samples did not exhibit sufficient thicknesses of feldspar overgrowths. Double side polished thick sections of these samples were cut into 10*8*0.8 mm chips. These chips were irradiated at the CLICIT facility of the Oregon State TRIGA Reactor (OSTR) at Oregon State University together with the sanidine age standard, FC3 (27.5 ± 0.2 Ma; Uto et al. 1997), from the Fish Canyon Tuff standard from the Geological Survey of Japan, focusing on K₂SO₄ and CaF₂ salts. Details on the irradiation procedure at OSTR can be found in Engelhardt et al. (2017). Ar isotope analyses by in-situ laser ablation were performed on K-feldspar detrital grains and overgrowths, with a UV pulse laser (wavelength of 266 nm) of the New Wave Research DualWave laser in most cases with 20–40 µm diameter and maximum energy of 0.3 mJ to ablate parts of the mineral. From 3 to 7 spots were analysed for each grain and overgrowth. The gas extracted by each ablation was then cleaned in SAES © getters, and a cold trap cooled by ethanol to -90 ˚C by the electric cooler on the ultra-high vacuum purification line. After 10 min of cleaning, the gas was transferred to the noble gas mass spectrometer Micromass 5400, then was analysed for 15 min by a 7-cycle series of argon isotope measurements to calculate the age of analysed segments of K-feldspar. A blank analysis was launched after analysis of a series of 3 acquisitions. Ar isotope analysis and calculation of ages and errors were conducted by MassSpec (Alan Deino Software).

Basin modeling

1D burial models were created with Petromod ®1D (Schlumberger). Burial scenarios were modelled based on the regional geological history and well data as boundary conditions. The modelling of the evolution of temperature with time is implemented for three locations of interest: Roemerberg and Soultz-sous-Forêts domains, representative of two localities in the central part of the basin, with a varying Tertiary burial sequence, and a third model for the shoulder domain (Burial sequence type listed on Table 1). The conditions of present thickness, erosion, deposition times, lithology, age, are available in supplementary data. Heat flow conditions are the same for the three burial scenarios (see supplementary material). The heat flow variation over time is extracted from Böcker et al. (2016), with two phases of increasing heat flow associated with hydrothermal and tectonic activity during Jurassic and Early Tertiary. The heat flow is calibrated on vitrinite reflectance from Liassic source rocks sampled within the URG and shoulders. The variations of the deposited thickness of post-Buntsandstein layers during the Mesozoic is due to differential erosion during the Late Triassic, which was more intense towards the NNW. These scenarios are tested and compared to the burial model outputs to have more insights in which periods and at which depth in correlation to the burial scenarios quartz cement may have formed.

We used the key relation between δ¹⁸O_quartz and the temperature, noted T (see Eq. (2) from Sharp et al. (2016). This equation was applied on the burial temperature curves modelled with PetroMod ® 1D, to estimate quartz cementation conditions from δ¹⁸O_quartz measured in overgrowths:

$$\frac{{4.28 \times 0.07 \times 10^{6} }}{{{\text{T}}}}~ - ~\frac{{3.5 \times 0.2 \times 1000}}{{\text{T}}} = ~1000 \times ~\ln ~(\alpha _{{quartz - H20}}^{~} )$$

(2)

Three different scenarios were tested with different types of isotopic fluid compositions, e.g., 0 %, + 5 %, and − 5 %, representing different sources of fluids: formation water, diagenetic water, and meteoric water, respectively (Smith et al. 1998; Cathelineau et al. 2004; Hyodo et al. 2014; Hoefs et al. 2015; Blaise et al. 2016).

Results

Petrography

Analysed samples classify as silts and fine-grained to coarse-grained sandstones, with grain diameter ranging from 30–50 to 850–900 µm. Some grains and pores exhibit a clay coating composed of illitic minerals, but grain to grain contacts do not show any clay coating, suggesting an authigenic origin of this first phase of clay coating. Quartz overgrowths are present in a large amount in the intergranular spaces, mainly developed on the largest detrital grains, whose surface is not coated by smectite or illite. The thickness of quartz overgrowths ranges from 20 to 200 µm. In CL, the colours of detrital quartz grains vary between red, brown and dark violet. Quartz overgrowths show several zonations highlighted by varying cyan-blue intensities for samples from the category F (Fig. 5). Some laminae present well-developed quartz overgrowths, with almost no compaction at the bedding scale. Feldspar overgrowths show no to very soft cyan cathodoluminescence, contrasting with the bright cyan luminescence of detrital feldspar (Fig. 6). The feldspar overgrowth thicknesses range from 30 µm up to a maximum of 80–100 µm. The intergranular pores are also partly occluded by platy illite.. This second illite texture is associated with authigenic apatite and partly covers quartz and feldspars overgrowths.

Fig. 5

Petrographic observations of quartz overgrowths on samples. A SEM–CL microphotograph of non-luminescent quartz overgrowth (white arrow) within the intergranular space. B SEM–BSE microphotograph of (A). C SEM–CL microphotography of blue luminescent quartz overgrowth (white arrow) on the right bottom corner of the picture, euhedral quartz overgrowths developed on the fracture plane, filled by siderite and barite. Quartz cements present zonings in CL. D SEM–BSE microphotograph of (C). E SEM–CL microphotograph of zoned quartz overgrowths (white arrow) within intergranular pores, filled with barite. F SEM–BSE microphotograph of (E). G SEM–CL microphotograph of zoned quartz overgrowths (white arrow) within intergranular pores, filled with barite. Zoned overgrowths are affected by healed cracks, cross-cutting detrital, and overgrowth quartz. H SEM–BSE microphotograph of (G)

Fig. 6

Petrographic observations of feldspar overgrowths on analysed samples. A SEM–CL microphotograph of a cemented bed, with syntaxial feldspar rim (white arrow) around detrital grains. B SEM–BSE microphotograph of a cemented bed, with syntaxial feldspar rim (white arrow) around detrital grain. C SEM–CL microphotograph of feldspar syntaxial cement on the border of a detrital grain. Porosity is partly cemented by barite. Feldspar cement is encased partly by quartz overgrowth. D SEM–BSE microphotograph of feldspar syntaxial cement on the border of a detrital grain. Porosity is partly cemented by barite. Feldspar cement is partly encased by quartz overgrowth. E SEM–CL microphotograph of a cemented bed, with syntaxial feldspar rim (white arrow) around detrital grains, and encased by a quartz overgrowth (red arrow). F SEM–BSE microphotograph of syntaxial feldspar cement (white arrow) on the border of a detrital grain and overgrown by illite crystals (green arrow)

Samples originating from the vicinity of faults present a partly cemented fracture network. The fracture cementation shows (1) quartz as overgrowths on detrital quartz grains along the fracture plane; (2) intergranular siderite cement encasing euhedral faces of formerly crystallised quartz and feldspar overgrowths (Sid1) (Fig. 6 A, B); (3) blocky to needle-shaped barite cement covering both euhedral quartz overgrowths and intergranular siderite (Fig. 6A, B, C and D); and 4) siderite fracture cement encasing barite needles (Sid 2) (Figs. 5 and 6C, D). In samples from buried reservoirs, siderite and barite cementation can be pervasive in the intergranular space within the fracture plane vicinity. Only samples from currently buried sandstone present both siderite and barite within the fractures. Samples from the URG shoulders present only barite cementation, which is mostly restricted to the fracture plane.

δ¹⁸O in detrital grains and quartz overgrowths

δ¹⁸O_detrital distributions are similar for the different samples, ranging from -3.2 to 21.2 %, with a peak of 8–12% (Table 2, Fig. 7).

Table 2 δ¹⁸O _quartz average data sorted by sample and differentiating detrital and overgrowth δ¹⁸O _quartz

Fig. 7

Histograms of δ¹⁸O _quartz values for the ten samples. Detrital grains are represented in white, and quartz overgrowth measurements in light red

δ¹⁸O _overgrowth varies from 11 to 26.1% (Table 2, Fig. 7).

Profiles of δ¹⁸O _overgrowth were established, showing a record of the variations of δ¹⁸O _overgrowth from the grain–cement boundary to the border of the cement rim. These profiles show two different evolutions in the δ¹⁸O composition of quartz overgrowth (Figs. 8, 9). Samples of the first group (A) present a monotonous decrease of the recorded δ¹⁸O _overgrowth from the spots closest to the detrital grain to the most recent cement (Fig. 8). The second type of pattern (samples from group B) shows chaotic variations in δ¹⁸O _overgrowth. For example, in sample F-3225, several profiles recorded an increase in δ¹⁸O from the earliest to the latest overgrowths (Fig. 9).

Fig. 8

δ¹⁸O _quartz variations within quartz overgrowths for samples of category C—intergranular non-disturbed behaviour

Fig. 9

δ¹⁸O _quartz variations within quartz overgrowths for samples of category F—fracture vicinity behaviour

In-situ ⁴⁰Ar/³⁹Ar age of K-feldspar detrital grains and overgrowths

The ages obtained from the K-feldspar overgrowths are distinguishable in two groups (Fig. 10): (a) a group recording an age from 250 to 230 Ma (± 15 Ma), that corresponds to a phase of early cementation during the deposition of the sandstones, i.e., 250 Ma. (b) a second group recording a later phase of growth, from 180 to 150 Ma (± 20 Ma).; which corresponds to mesodiagenetic cementation.

Fig. 10

A ⁴⁰Ar/³⁹Ar ages of K-feldspar in samples, distinguishing detrital K-feldspars (grey) and K-feldspar overgrowths (purple). B Details on overgrowths

Basin modelling

The burial curves resulting from the 1D basin modelling (Fig. 11) are used to test several hypotheses on the δ¹⁸O_fluid from the modelled temperature curves.

Fig. 11

1D burial curves for the three scenarios modelled: A URG shoulder outcrop configuration. B Soultz type configuration with moderate burial during Oligocene. C Roemerberg type configuration with deep-seated reservoirs due to tertiary burial sequence

From deposition (250 Ma) to the Norian (Upper Triassic), the regime of subsidence is similar for all the localities. A regional erosional phase, affecting the Upper Triassic and Middle Triassic deposits, characterises the Norian unconformity. This erosional phase and the diachronic sedimentation onset during the Jurassic explains the variability of the Mesozoic burial sequences.

A regional uplift leads to the progressive erosion of the sedimentary deposits from the Upper Cretaceous up to the Late Paleocene (Schumacher 2002; Cloetingh et al. 2006), with eroded thicknesses estimated up to 1 km during the Cretaceous (Böcker and Littke 2015).

With the rift opening starting during the Eocene, the burial depth varies depending on the location within the basin. Sequences on the rift shoulders (e.g., illustrated in Fig. 11A) were slightly buried during the Eocene and the Oligocene. The Cenozoic sedimentary deposits are reaching their maximum thickness of nearly 400 m during the Miocene. Rift shoulders undergo a second uplift, resulting in the erosion of the Cenozoic deposits and the remaining Mesozoic sequence up to the Buntsandstein Gp..

On the first blocks inside the rift, as illustrated by the case of the Soultz horst (Fig. 11B), the Cenozoic burial sequence starts during the Eocene. It continues with an increase of burial depth during the Oligocene (up to 1500–2000 m for the Buntsandstein Gp. bottom line). The Miocene uplift slightly affects the sedimentary column, with the erosion of a few tens of meters of deposits during the Tertiary.

Finally, the third configuration is illustrated by the Roemerberg case (Fig. 11C), with two majors Cenozoic subsidence phases, during the Oligocene and the Early Miocene. The Late Miocene uplift phase leads to the erosion of approximately 100 m of Tertiary deposits. This third configuration is when Buntsandstein Gp. sandstones reach their maximal burial depth during the Cenozoic. For the two previous configurations, burial reaches its maximum during the pre-rift burial phase.

Following the diagenetic sequence (Fig. 12), Eq. 3 is applied to these modelling results to retrieve an age and a hypothetical δ¹⁸O_overgrowth from modelled temperature and fixed δ¹⁸O_fluid compositions (Fig. 13) to discuss the cementation timing.

Fig. 12

Paragenetic sequence within the Buntsandstein Gp. sandstones. Two paragenetic sequences are established, one for deep-seated sandstones and one for sandstones from outcrops. In grey, the diagenetic sequence affecting the sandstone before the deformation; in dark green, events affecting the fracture network and surrounding intergranular space; in light green, potentially dissolved siderite phases. Reference for dating a (Blaise et al. 2016), b (Schleicher et al. 2006)

Fig. 13

A δ¹⁸O_overgrowth: (1) calculated from temperature evolution during simple basin burial (blue line) and (2) calculated from temperature evolution during burial coupled to fault fluid-flow within sandstones (orange dashed line). B Profiles in a sample recording mainly burial evolution. C Profiles in a sample recording mainly the fluid flow. D Diagram of the evolution of δ¹⁸O overgrowth versus the temperature for three modelled δ¹⁸O fluid values (− 5% meteoric, 0% initial formation water, + 5% diagenetic), and associated ranges encountered in samples

The first scenario considers a fluid with a constant isotopic signature of 0%.

This first scenario suggests that observed δ¹⁸O_overgrowth could form starting from 200 Ma (Fig. 13A) from 50 to above 180 °C.

By testing the second source of a fluid with constant isotopy =  + 5%, δ¹⁸O_overgrowth could form from 90 to above 200 °C.

By testing the third source of a fluid with constant isotopy = − 5%, δ¹⁸O_overgrowth could form from 30 to 150 °C.

Discussion

The new results obtained on the isotope composition of quartz and K-feldspar allows insights into the origin of detrital grains and their overgrowth cement, potential sources for silica, fluid origin, and temperature of mineralisation. These outputs improve the understanding of the basin dynamics and fluid flow episodes in the URG.

Provenance of detrital grains.

Values of δ¹⁸O_detrital measured within the detrital quartz grains are similar for all the samples. The values of δ¹⁸O_detrital (mean: 8–10%) for analysed samples suggest an igneous origin (Valley and Graham 1996; Götze et al. 2012; Hyodo et al. 2014). The lowest values, around 0%, likely originate from a low-δ¹⁸O magma. The diversity of colours in cathodoluminescence from blue to violet shades and red may reflect multiple igneous origins, the minor amount of red grains from volcanic quartz, and a majority of blue and violet for metamorphic and plutonic quartz (Richter et al. 2003; Götze et al. 2012). The highest values of δ¹⁸O_detrital (16–21%) can be linked to redeposited grains with a previous quartz overgrowth, likely from sandstones from the Grès Armoricain Fm. (Gloaguen et al. 2007; Tartèse et al. 2015). These observations are consistent with the ones presented by Soyk (2015) on samples from the Buntsandstein Gp.. The origin of detrital quartz grains of these Lower Triassic sandstones was located to the West (Köppen and Carter 2000) near the southern border of the Armorican Massif, which was eroded during the Permian and Triassic (Ballèvre 2016).

The ⁴⁰Ar/³⁹Ar ages measured in detrital K-feldspars show a Carboniferous age for the majority of grains. These ages coincide with the Variscan orogeny, during which plutonic rocks formed in the Armorican, Vosges, Black Forest, and Rhenish massifs. Sedimentary Pre-Variscan basement, which underwent metamorphism, is associated with the oldest feldspars dating from 800 Ma. The collapse of the Variscan belt and the relief erosion is the source rock for detrital grains forming the Buntsandstein Gp. sandstones (Bourquin et al. 2006, 2009, 2011).

Argon isotopy and diagenetic paragenetic sequence.

A 4 stages paragenetic sequence is defined for the Buntsandstein Gp. sandstones, with late-stage variations depending on their structural location (Fig. 12).

(1) Formation of a detrital smectite/illite grain coating, and for some samples, the first phase of eodiagenetic K-feldspar cementation occurs in the very early stages of diagenesis (first peak of Ar/Ar ages distribution around 250 Ma) (Fig. 10).

(2) Quartz overgrowths develop around detrital quartz grains and encase some of the preexisting feldspar overgrowths.

(3) The second generation of K-feldspar overgrowths, with ages ranging up to 150 Ma, develops around quartz overgrowths and detrital feldspar grains, with ages ranging up to 150 (Fig. 10).

The Ar/Ar isotopic content can distinguish the two generations of K-feldspars overgrowths. Phases (2) and (3) can be concomitant (Fig. 12).

(4) The fourth step is the precipitation of an authigenic phase of illite, which covers the euhedral quartz overgrowths. This part of the paragenetic sequence is the same for all locations sampled in this study and is similar to the previously published regional paragenetic sequence for these sandstones in the URG area (Haffen 2012; Soyk 2015; Blaise et al. 2016; Bossennec et al. 2018). Such results suggest a common burial history at the regional scale. The illitisation is accompanied by partial dissolution of K-feldspars (both detrital and overgrowths) in the analysed samples. According to previous studies, the illitisation of K-feldspar started to develop in the Buntsandstein Gp. sandstones, for the URG, approximately 180 Ma (Liassic), lasting until approximately 150 Ma (Late Jurassic–Early Cretaceous) (Clauer et al. 2008; Blaise 2012). The youngest ages recorded in K-feldspar overgrowths are contemporaneous with the last steps of illitisation. During the Late Jurassic, several hydrothermal events are also recorded in the area, leading to hot fluid flow and extensive precipitation of authigenic illite around fault zones, recorded in various formations of the Mesozoic sedimentary deposits, in the area of the future URG (Meyer et al. 2000; Brockamp and Clauer 2005; Cathelineau et al. 2012; Blaise et al. 2016). This generation of authigenic illite, present in the damage zones of faults; is recognised in several localities around the URG, suggesting a regional fault activation. Because K-feldspars analysed are partly dissolved, and due to the relatively smaller size and thickness of the analysed overgrowths around the detrital grains, these conditions did not allow us to perform measurements with higher precision than ± 15 Ma. Indeed, the errors of ⁴⁰Ar/³⁹Ar ages on the K-feldspar increased when the spots' size was smaller. As the laser spot size is decreased, less material is evaporated, reducing the overall signal amplitude. However, the interpreted ages give a first order of the timing at which K-feldspar cements crystallised. Two Ar/Ar age peaks are determined, suggesting two generations of K-feldspar overgrowths, which fit within the already published sequence and timing for illitisation. Here, K-feldspar overgrowth generation (1) predates the illitisation, and K-feldspar overgrowth generation and (2) concludes in the same time frame in which other studies recorded the first illitisation ages (Schleicher et al. 2006; Clauer et al. 2008; Brockamp et al. 2011).

The paragenetic sequence diverges in the late stage during the Cenozoic rift opening, with siderite and barite cementation on samples within buried sandstones. Samples from the URG shoulders present only barite. Dissolution of carbonates by meteoric waters, from which Fe–Mn oxides stains are remaining, potentially explains the lack of siderite in outcrop samples (Soyk 2015).

Source of silica for pore network cementation

Quartz cementation in sandstones can have various silica sources within the sedimentary basins (Saigal and Morad 1988; Worden and Burley 2003; Bjørlykke 2014). Internal sources could have included biogenic silica in sandstones. However, as no biogenic silica is observed, silica sources restrain to classical diagenetic reactions products. Some of the quartz overgrowths in the observed samples show bright blue and dark violet zonations under hot CL. These bright blue CL emissions are induced by Al³⁺, which substitutes Si⁴⁺ (Boggs and Krinsley, 2006; Götte et al. 2013; Götze et al. 2012). Two primary sources could be suspected as aluminium is a product of the albitisation of K-feldspars (Mark et al. 2005; Lander and Bonnell 2010; Xi et al. 2015). Albitisation also releases silica (Brosse et al. 2000; Mansurbeg et al. 2008; Xi et al. 2015). K-feldspar is poorly albitised in studied samples. Illitisation of detrital K-feldspars could be the second source for Al (Lanson et al. 2002; Lander and Bonnell 2010; Götte et al. 2013). K-feldspar grains show very scarce illitisation, restricted to detrital grain boundary and transgranular cracks surface. However, most of the felspar grains remain unaltered, except in deep-seated reservoirs in Roemerberg within the vicinity of fault systems. According to the observations of relatively well-preserved feldspars, except within fault zones, it is likely that pore water remains saturated in K⁺, SiO₂, and Al, which also allows the growth of K-feldspars overgrowths (Lanson et al. 2002). Fluids enriched in Al, K⁺, and SiO₂, if sourced from K-feldspar transformation, should then have an external origin (Yuan et al. 2015) and could be drained to the sandstones more efficiently within the fault damage zone, as shown in a previous study (Bossennec et al. 2018). From damage zones, fluids may percolate through the porous sand bodies, from volumes, where albitisation took place, i.e., fault zones within the crystalline basement (Brockamp et al. 2003; Brockamp and Clauer 2005; Schmidt et al. 2017). The illitisation of clay mineral grain coatings may also provide an internal silica source (Yang 2000; Tournier 2010; Zhu et al. 2015). The illitisation of smectites, for example, can affect the isotopic composition of the pore fluid by increasing δ¹⁸O_fluid from + 2 to + 5 % (Tournier et al. 2010; Pollington et al. 2011; Hyodo et al. 2014).

Chemical compaction is another potential internal source of silica and is well marked in fine grain-sized laminae of Buntsandstein Gp. sandstones (Haffen et al. 2015; Soyk 2015; Schmidt et al. 2020). The pore fluid mediates the effect of compaction on the value of δ¹⁸O_fluid. SiO₂ dissolves in the water, and the isotope composition is re-equilibrated. When SiO₂ precipitates, the δ¹⁸O composition is then a function of δ¹⁸O_fluid and temperature.

Massive illitisation in claystones and shales from different sedimentary formations or feldspar illitisation in the crystalline basement releases silica into the circulating brine. The migration from this external brine into the sandstone reservoir is enhanced by fault activity, usually allowing fluid migration within the fault damage zones.

No clear distinction can be deciphered regarding the silica source. Likely candidates are feldspar dissolution (partial in areas weakly affected by fault systems), feldspar illitisation, increased in the vicinity of a fault zone, chemical compaction of detrital quartz grains, and clay mineral recrystallisations, which can commonly be observed in sandstone diagenesis (Worden and Morad 2000; Wilkinson 2001; Worden and Burley 2003; Tournier et al. 2010).

Fluid typing and temperature of mineralisation

Although the burial sequences are different during the Cenozoic for sandstones located on the graben shoulders and in the centre of the basin, the range of recorded δ¹⁸O in the quartz overgrowth is similar for the entire data set, with the highest values registered at 26% and lowest values of 12%. This homogeneous range is an argument for the initiation of quartz cementation during the Late Triassic and Jurassic. These profiles can result from two settings of quartz cementation conditions:

A monotonous decrease of δ¹⁸O_overgrowth from the contact with the detrital grain to the cement border characterise the first regime of quartz cementation (Figs. 8, 13). Even if none of the overgrowths analysed show the record of a complete burial sequence, the assemblage of the several profiles for each sample is covering the interval of δ¹⁸O on quartz, which can be related to a continuous burial phase and quartz precipitation during the Mesozoic (Harwood et al. 2013). Values of profiles in this regime range from 26 to 16%.

The second quartz cementation regime is observed on samples collected in the damage zones of faults (Figs. 9, 13) and on overgrowths that present bright blue zonings in CL analyses. For these samples, the analysed profiles present a chaotic pattern of δ¹⁸O variation within the quartz overgrowth. The values of δ¹⁸O are lower than those for the previous regime. Here, δ¹⁸O ranges from 19% to 12%. Overall, samples from category F have lower values of δ¹⁸O registered in quartz overgrowths. The fluctuations observed in this second type of profile could be connected either to very local temperature variations or variations of the fluid types due to fault activity and fluid transfer within faults, disturbing the geochemical conditions locally.

One means of estimating the minimum mineralisation temperatures and the nature of the fluids is micro-thermometry. Unfortunately, the overgrowths analysed in this study, even from thick sections, do not have inclusions large enough to be analysed (micron to submicron size). Previous studies on fluid inclusions in quartz overgrowths provide insights into fluid type and source variations within the basin and at the basin-basement interface (Dubois et al. 1996; Smith et al. 1998; Boiron et al. 2011; Gardien et al. 2016).

The oxygen isotopic signature aids the identification of the fluid origin. Three sources of fluid are differentiated. Generally, positive δ¹⁸O_fluid from + 2 to + 5 % is associated with the release of waters during the illitisation of clays (Cathelineau et al. 2004; Hyodo et al. 2014; Blaise et al. 2016). Hot meteoric fluids involved in hydrothermal mineralisation in the area also have a peculiar signature, with a negative δ¹⁸O_fluid, ranging from − 10 to − 5 % (Zwingmann et al. 1999; Hoefs et al. 2015). Currently, formation waters sampled within the Buntsandstein Gp. sandstones have a δ¹⁸O_fluid ranging from − 1.1 to − 2.9 % (Sanjuan et al. 2016). The range of δ¹⁸O _overgrowth is not only explained by pure temperature variations with time. It is, therefore, necessary to test different scenarios (Fig. 13).

The first scenario considers a fluid with a constant isotopic signature of 0%, reflecting a fluid similar to Buntsandstein Gp. formations waters at the time of deposition. For this value, quartz cementation starts at 50 °C for the first profiles. It continues monotonically up to temperatures of 130–140 °C for samples outside of damage zones (Fig. 13), following the burial models (Fig. 11). This fluid hypothesis fits the majority of the measured values, other fluid sources or higher temperature could explain the lower values of δ¹⁸O _overgrowth. The record of the monotonous burial of the Buntsandstein Gp. sandstones corresponds to previous results, using other burial markers, as vitrinite reflectance (Blaise et al. 2014, 2016; Böcker et al. 2016).

The second scenario tests a fluid with constant isotopy =  + 5%, which represents a diagenetic origin. The calculated temperatures show a start of quartz cementation at 90 °C and up to more than 250 °C. The start of cementation at 90 °C is plausible due to the improved kinetics of quartz cementation at temperatures above 80 °C (Bjørlykke et al. 2004). However, the temperatures calculated for the terminal part of the profiles (> 180 °C) are inconsistent with the geological history. This source explains the smallest number of measurements for the expected burial conditions, and other fluid sources and crystallisation temperatures must be expected.

By testing the third source of a fluid with constant isotopy = −5%, the temperatures obtained by calculation are not ideal for the monotonically decreasing profiles (beginning at 50 °C and rising up to 120 °C). However, they explain the decreases and fluctuations recorded by the samples exhibiting chaotic profiles near the faults.

The combination of these three scenarios allows defining a frame for fluid isotopic signatures and their evolution. Overall, for the first overgrowths with values above 20 % (the closest to the grain boundaries),the main domain for fluid typing is comprised between 0 and slightly negative δ¹⁸O _fluid (Fig. 13D). Fluid inclusion studies (Soyk, 2015) associate these first overgrowths with a homogenisation temperature (T_h) of 50 °C, concordant with a fluid composition around 0 %, and mineralisation linked to a meteoric or a sedimentary fluid. Tm_ice ranges vary, suggesting two possible origins, e.g., meteoric for low salinity fluids (Tm_ice above -5 °C) and more saline brines from sedimentary fluids. The salinity can also vary in a single cementation phase due to heterogeneous trapping (Cathelineau and Boiron 2010).

Following the onset of quartz cementation, with the first decrease of δ¹⁸O, the next-coming increase of δ¹⁸O registered in sample profiles can thus be associated to a) a decrease of temperature, with uplift, while there is no hot fluid flow, the temperature returns to the global burial temperature at this depth or b) fluid flow with a δ¹⁸O_fluid isotopic signature above 0 %. Fluids containing solutes from illitisation reactions are fluids that can match this scenario, as their isotopic δ¹⁸O_fluid is usually higher than 2%. This variability of the isotopic composition of fluids is associated with fluid-mixing processes, as underlined by salinity variations in quartz mineralisations in fault zones, such as in the Soultz granite (Dubois et al. 1996; Smith et al. 1998; Cathelineau and Boiron 2010) or in the Schwarzwald (Staude et al. 2009; Pfaff et al. 2010).

A combination of a) and b) is also possible, as sedimentary brines from overlying layers might also be cooler.

The intermediate and most numerous values of δ¹⁸O _overgrowths (between 15 and 20 %) are associated with higher δ¹⁸O_fluid. This increase of δ¹⁸O _fluid is related to the high δ¹⁸O _fluid released by illitisation. This illitisation of smectitic clay grain coatings is enhanced in the fault vicinity, as suggested by the chaotic profiles.

The next generations of fluid inclusions analysed in quartz overgrowths by Soyk (2015) show T_h around 150 °C. These FI are characterised by low salinity (T_mice above − 5 °C), which could mark the higher contribution of meteoric fluids infiltrated in the deep basement on quartz cementation in the Buntsandstein Gp sandstones. This second phase of quartz cementation is recorded regionally (Smith et al. 1998; Dubois et al. 2000; Cathelineau and Boiron 2010). The fluid should have a δ¹⁸O _fluid ranging from 0 to − 5 % to reach the obtained values of the latest δ¹⁸O _overgrowths (below 15%) at 150 °C. This estimated value for δ¹⁸O _fluid is typical for present-day meteoric fluids. Hot meteoric fluids related to fault activity are good candidates because of their isotopic δ¹⁸O_fluid between − 10 and − 5 %, their low salinity, and the high temperature of the fluid (> 180 °C) (Schwinn et al. 2006; Baatartsogt et al. 2007; Pfaff et al. 2010; Boiron et al. 2011; Brigaud et al. 2020).

Conclusions

In situ analysis of oxygen isotopic ratios provides an analytical tool to decipher the sources of detrital and authigenic quartz. The average δ¹⁸O_quartz compositions of detrital grains suggest a predominantly igneous origin. Quartz overgrowths present two categories of profiles. The first category of profile records the monotonous decrease of δ¹⁸O_overgrowth, and is related to the Mesozoic burial sequence. The second category of profile has a more chaotic pattern. This profile shape is explained by the variations of the temperature range, eventually locally associated with a variation of the fluid isotopic composition in the vicinity of faults.

The proposed burial and paragenetic sequence can be summarised in two phases and associated geological processes:

1) The first phase of cementation occurs during a monotonous burial, from ~ 180 Ma up to ~ 150–140 Ma.

2) The second phase of quartz cementation is linked to the first episodes of deformation and fluid flow starting from the Early Jurassic and associated with the hot fluid pulses responsible for regional illitisation. The record of δ¹⁸O_overgrowth is chaotic due to the interaction between several types of external fluid sources, with a mix of hot hydrothermal fluids and co-generated ¹⁸O-enriched illitisation fluids, which would explain the widespread strong zonation observed in quartz overgrowths associated with these chaotic profiles.

These signal disturbances recorded in the overgrowths are likely to be posterior to the regional burial phase recorded by the first type of profile. Before the Cenozoic rift opening, quartz overgrowths form prior to authigenic illite dated from the Late Jurassic to Paleogene. This modelling also correlates with the absolute in-situ ⁴⁰Ar/³⁹Ar dating results obtained on the feldspar overgrowths, with the youngest ages corresponding to 140 Ma, i.e., in the late Jurassic period.

This study indicates that most of the intergranular pore network cementation ceases before the deformation associated with the rifting phase during the Eocene. The first phases of deformation impact the latest phases of quartz cementation, as recorded in the disturbance of the isotopic signature of quartz overgrowth in the vicinity of fractures.

Based on the analysis of δ¹⁸O on quartz overgrowths, the diagenetic history recorded is very similar for the entire study area, with the same ranges of values recorded on the graben shoulders and the buried parts of the basin. This study shows the importance of understanding the fault system activity during the reservoir geological evolution. Here, the pore network modification due to cementation mostly predates the basin structuration in blocks. Similar intergranular pore network diagenesis could be expected for reservoir blocks unaffected by faults, not depending on the current burial position.