Rift thermal inheritance in the SW Alps (France): insights from RSCM thermometry and 1D thermal numerical modelling
Conceptual models of orogenic accretionary prisms assume that peak temperatures (Tmax) increase towards the internal domains as crustal rocks are accreted from the lower to the upper plate. However, the recognition of pre-orogenic heating events in mountain belts questions the magnitude of thermal overprint during nappe stacking. Using Raman spectroscopy on carbonaceous material (RSCM) to calculate Tmax, we have investigated the thermal record of Lower Jurassic to Eocene strata exposed along six stratigraphic sections at the front of the Digne Nappe (SW Alps), from the Devoluy Massif to the Castellane Arc. Our results highlight two groups of depth-dependent temperatures: (1) a regionally extensive and constant Tmax up to 300–330 ∘C measured in the Jurassic succession and (2) regionally variable lower temperatures (<150 ∘C) recorded either in the Upper Mesozoic or the syn-orogenic sequence. Modelling shows that the highest palaeotemperatures were achieved during the Early Cretaceous (∼ 130 Ma), associated with the Valaisan–Vocontian rifting, while the lowest Tmax reflect post-rift thermal relaxation in the Alpine foreland basin. This study provides a striking new example where mid-crustal palaeotemperatures measured in sediments accreted from the downgoing plate are inherited. An estimated peak thermal gradient of 80–90 ∘C km−1 requires a crustal thickness of 8–10 km during the Early Cretaceous, hence placing constraints for tectonic reconstruction of rift domains and geophysical interpretation of current crustal thickness in the SW Alps. These results call for the careful interpretation of palaeothermal data when they are used to identify past collisional thermal events. Where details of basin evolution are lacking, high-temperature records may be misinterpreted as syn-orogenic, which can in turn lead to an overestimation of both orogenic thickening and horizontal displacement in mountain belts.
The identification of collisional events through Earth's history lies in our capacity to distinguish in the rock record and crustal structure the effect of crustal thickening among other tectono-magmatic events unrelated to plate convergence. Conceptual models of orogenic accretionary prisms describe the increase of peak temperatures (Tmax) from the external fold-and-thrust belts to the internal high-grade metamorphic domains as a result of tectonic burial heating and thermal advection due to nappe stacking and erosion as crustal rocks are accreted (Barr et al., 1991). Therefore, a potentially relevant indicator of collision is the onset of heating related to crustal thickening of previously subducted rocks (e.g. Soret et al., 2021). However, it has been shown that mid-crustal temperatures (i.e. at least 300 ∘C) reconstructed in accreted sedimentary rocks can represent rift-related thermal peaks not overprinted by crustal thickening. This has been substantiated in low-convergence collisional orogens, such as the Pyrenees (Izquierdo-Llavall et al., 2020; Vacherat et al., 2014; Clerc and Lagabrielle, 2014; Ducoux et al., 2021) and the Iberian Range (Rat et al., 2019) as well as in higher convergence collisional orogens, such as Taiwan (Conand et al., 2020). In the Alps, the preservation of pre-Alpine contacts in high-pressure metamorphic units formed during the development of the European margin of the Alpine Tethys (e.g. Beltrando et al., 2014) and the current debates regarding the interpretation of pressure–temperature–time paths (Pleuger and Podladchikov, 2014; Luisier et al., 2019; Schmalholz and Podladchikov, 2013), have raised questions about the magnitude of continental subduction and the role of precollision evolution on the orogeny dynamics. Therefore, we need to improve quantification of pre-orogenic versus syn-orogenic thermal evolution in orogenic wedges to reduce uncertainties on tectonic reconstructions and recognition of past collisional events.
The Western Alps are an archetypal mountain belt formed by the crustal accretion of the palaeomargins of Europe and Adria that followed the subduction of the Alpine Tethys (e.g. Handy et al., 2010). The Tmax of about 300 ∘C reported from Raman spectroscopy on carbonaceous material (RSCM) and mineral thermometry in accreted sediments of the European plate (e.g. Briançonnais and Schistes Lustrés units; Fig. 1) are commonly attributed to syn-convergence thermal overprint in the internal units (e.g. Gabalda et al., 2009; Lanari et al., 2012). The RSCM temperatures estimated in precollision Mesozoic sediments of the external units are also close to or above 300 ∘C and have been interpreted as reflecting burial of the European margin beneath the internal units of the belt (Deville and Sassi, 2006; Bellanger et al., 2015). However, these mid-crustal temperatures are at odds with the expected decrease of tectonic burial in the external parts of orogenic accretionary wedges and may instead reflect a thermal event prior to collision, a possibility that is yet to be assessed.
Here, we focus on the Digne Nappe, characterised by a thick Mesozoic-Cenozoic section transported above the Digne thrust, at the front of the external SW Alps (e.g. Gidon, 1997). The low apparent internal deformation makes this region suitable for deciphering the thermal impact of rifting events from other tectonic phases. This study combines 90 new RSCM measurements from samples collected at the front of the Digne Nappe along continuous stratigraphic successions that recorded, prior to the onset of nappe emplacement, the evolution of the European margin from the opening of the Alpine Tethys until the early stages of the Alpine foreland. To resolve the timing of pre-orogenic versus syn-orogenic thermal imprints, a set of modelled time–temperature scenarios has been designed. Our results lead to the re-evaluation of the importance of rifting-related, lower plate thermal inheritance, and provide constraints on the palaeogeography and rift architecture in the SW Alps.
The SW Alps comprise five tectono-stratigraphic domains (Fig. 1). From NE to SW these are: (1) the Internal Crystalline Massifs that represent the crust of the stretched European margin subducted and rapidly exhumed in Eocene times; (2) the Liguro–Piemont domain, made of Jurassic to Paleocene metasediments of the Schistes Lustrés complex that originated from the oceanic floor and continent–ocean transition of the Alpine Tethys; (3) the continental block of the Briançonnais and sub-Briançonnais domains, made of Paleozoic, Mesozoic and Cenozoic metasediments characterised by limited crustal thinning during the Alpine Tethys opening; (4) the Upper Cretaceous–Paleocene Helminthoid flysch of the Embrunais–Ubaye nappes with slices of Briançonnais and sub-Briançonnais units at their base, and (5) the Dauphinois–Helvetic domain, which forms the external Alps, to the west of the Penninic front, and characterised by the External Crystalline Massifs and by Paleozoic, Mesozoic and Cenozoic sediments constituting the external fold-and-thrust belt (Fig. 1b).
In the Western Alps, kinematic reconstructions of the Alpine Tethys involve two different oceanic domains and/or hyperextended margins separated by the Briançonnais continental block: the Alpine Tethys sensu stricto and the Valaisan Domain (e.g. Stampfli and Borel, 2002). In the east, the Alpine Tethys opened during the Middle to Late Jurassic as attested by the ages of mafic rocks ranging from 166 to 155 Ma (e.g. Manatschal and Müntener, 2009). The continental break-up resulted in the formation of the slowly spreading oceanic domain of the Alpine Tethys oriented NE–SW between the European and Adriatic margins (Mohn et al., 2014; de Graciansky et al., 1989; Lemoine et al., 1986; Manatschal et al., 2021). In the west, the nature and the age of stretching of the Valaisan Domain, located between the Briançonnais and the Penninic front is more controversial. Ages span from (1) the Late Jurassic based on crystallisation age of a metagabbro (161 Ma; Liati et al., 2005) and indirect evidence of pre-Cretaceous mantle exhumation, to (2) the Early Cretaceous (130-90 Ma) as suggested by U–Pb dating of metamorphic zircon U-rich rims (Beltrando et al., 2007) and the interpretation of the Barremian–Aptian succession as post-rift deposits synchronous with the onset of oceanic spreading (Loprieno et al., 2011). These two contrasting views do not contradict evidence that the initiation of rifting occurred during the Early Jurassic in the Dauphinois Domain (e.g. Lemoine et al., 1986), leading to the development of a necking zone since the Pliensbachian in the External Crystalline Massifs (Mohn et al., 2014; Ribes et al., 2020; Dall'Asta et al., 2022). Thus, we consider the formation of the European margin to be a long-lasting process. Rifting started in the Early Jurassic and then evolved from the Late Jurassic into a hyperextended margin and slowly spreading ridge in the Alpine Tethys. During the Early Cretaceous, a distinct thermal, metamorphic and magmatic event occurred in the Valaisan Domain (Fig. 1c). The Early Cretaceous events appear to be synchronous with the renewed extension in the so-called Vocontian Domain (Fig. 1a and b), the SW Alps and the Provence platform (Fig. 1b) (de Graciansky and Lemoine, 1988; Hibsch et al., 1992; Jourdon et al., 2014; Angrand and Mouthereau, 2021).
Oceanic spreading lasted until the Late Cretaceous when the subduction of the eastern part of the Alpine Tethys started (Handy et al., 2010; Coward and Dietrich, 1989). Convergence in the Western Alps is characterised by two major stages (e.g. Ford et al., 2006). The first one, which occurred during the Eocene (55–34 Ma) reflects a period of subduction and rapid exhumation as the Alpine accretionary prism moved to the N-NW (Dumont et al., 2012, 2011; Merle and Brun, 1984; Lanari et al., 2014). The second stage occurred in the Late Eocene–Early Oligocene (34–30 Ma) and corresponds to the onset of widespread crustal thickening and collision in the Western Alps. This event is characterised by the onset of W–SW-oriented shortening in the southern Western Alps resulting in the deposition of Alpine foreland deposits during the Priabonian–Rupelian stage (Bellahsen et al., 2014; Dumont et al., 2011; Fry, 1989; Coward and Dietrich, 1989; Simon-Labric et al., 2009).
Structuring the foreland between the Variscan, Pelvoux and Argentera crystalline massifs, the Digne main thrust front is oriented NNW–SSE and dies out to the north near the western border of the Pelvoux (Fig. 1a). It turns to an E–W direction in the Castellane Arc to the south (Fig. 1b). To the east, the units of the Digne Nappe are overthrusted by the Embrunais–Ubaye (E-U) nappes emplaced at around 30 Ma, during and shortly after the deposition of the Eocene–Oligocene foreland deposits (Kerckhove and Thouvenot, 2010).
The Digne Nappe is made of Triassic to Cretaceous sediments that consist mainly of alternating limestones and marls (Fig. 1c) and Eocene–Oligocene foreland remnants made of Nummulitic limestones, Globigerina marls and continental sandstones and conglomerates (Fig. 1c) transported towards the SW over 20–25 km (Gidon, 1997; Faucher et al., 1988; Lickorish and Ford, 1998). These successions belong to the former European passive margin (Gidon, 1997; Baudrimont and Dubois, 1977; Debrand-Passard et al., 1984) and have been affected by salt tectonics since the Early Jurassic including the syn-orogenic phase (e.g. Célini et al., 2020, 2021, 2022). As the margin was inverted during the Miocene, Triassic evaporites provided an efficient décollement level for the Digne Nappe (Gidon and Pairis, 1986; Gidon, 1997; Faucher et al., 1988; Lickorish and Ford, 1998). The latest thick-skinned phase of deformation of the Digne Nappe, which is detected on seismic tomographic images as a major crustal-scale thrust (Nouibat et al., 2022), occurred during the Mio-Pliocene since ca. 10 Ma (Ford et al., 2006; Schwartz et al., 2017).
3.1 RSCM thermometry along reconstructed vertical sections
The RSCM approach is based on the temperature-dependent and irreversible natures of carbonaceous material (CM) maturation (e.g. Henry et al., 2019). The Raman spectra of CM change with increasing temperature so that a given spectrum thus reveals the Tmax experienced by a CM-rich rock through its history (Fig. 2). Several calibrations for the use of the RSCM thermometry, corresponding to various ranges of temperatures and geological contexts, were published (e.g. Beyssac et al., 2002; Rahl et al., 2005; Aoya et al., 2010; Lahfid et al., 2010; Kouketsu et al., 2014; Schito et al., 2017). The RSCM approach has been successfully applied to calculate Tmax in CM-rich rocks and infer the tectono-thermal histories of mountain belts and sedimentary basins (e.g. Gabalda et al., 2009; Conand et al., 2020; Ducoux et al., 2021).
For this study, the RSCM analyses were performed at the Bureau de Recherches Géologiques et Minières (BRGM) (Orléans, France) using a Renishaw inVia Reflex microspectrometer with a diode-pumped solid-state laser source excitation of 514.5 nm. The laser power that reached the surface of the sample, using a Leica DM2500 microscope and a ×100 objective (numerical aperture 0.90), never exceeded 0.1 mW. For each day of measurement, the microspectrometer was calibrated with a 520.5 cm−1 line of an internal silicon standard. The Rayleigh diffusion was eliminated by edge filters, and the Raman signal dispersed onto an 1800 lines mm−1 monochromator before analysis by deep depletion CCD detector (1024×256 pixels). For each sample, 10–15 measurements were acquired for data consistency, whenever the quality of the sample allowed it.
We selected 2.5–5 km thick (n=6) stratigraphic sections named DEV (Devoluy), SLC (La Saulce), CSN (Cousson), DGN (Digne), CLN (Coulnier), and CAS (Castellane) (Fig. 3) distributed from NNW to SSE over a distance of 80 km along the Digne thrust front (Fig. 1b). A total of 63 samples have been retrieved from precollisional carbonate deposits of Early Jurassic to Late Cretaceous ages, and 2 in Eocene foreland deposits (CAS and DGN, Fig. 3a). The sampled sections are assumed to represent the original vertical stratigraphic sections in the Alpine foreland basin prior to nappe emplacement in the Mio-Pliocene. This dataset was complemented by 15 RSCM analyses in the autochthonous units, in the E-U nappes and the Embrun half window (Fig. 1b and d). We applied the RSCM calibration of Lahfid et al. (2010) for temperatures ranging between 200 and 340 ∘C, and added the qualitative analysis of Saspiturry et al. (2020) for lower temperatures between 100 and 200 ∘C (Fig. 2).
3.2 Numerical modelling with basin model
To quantitatively examine which tectonic scenario best reproduces the distinct groups of depth-dependent temperatures observed along the Digne thrust front, we used 1D numerical modelling with TemisFlow® (Doligez et al., 1986). This basin modelling code simulates, among other processes, the compaction of the porous medium and heat transfer during a basin history. These physical phenomena are modelled by a set of partial differential equations representing the temperature equation, the mass balances of the solid and the water phases, coupled with a compaction law (Schneider et al., 2000). Heat transport uses as input: basal heat flow computed from a time evolutive 3-layer lithosphere model, surface palaeotemperatures, thermal conductivity of formations in the stratigraphic column and burial history, including erosion events. Both evolution of the crustal thicknesses linked to rifting events and erosion thicknesses were the parameters used to match the Tmax data.
Three scenarios have been tested.
The temperatures are only due to burial throughout the Mesozoic and Cenozoic without additional heat induced by lithospheric thinning (No-rift model).
The temperatures reflect the advection of heat during crustal and mantle thinning that resulted from the Alpine Tethys rifting event in the Early–Middle Jurassic (201–169 Ma), followed by a period of cooling after 125 Ma caused by thermal relaxation, i.e. the lithosphere–asthenosphere boundary (LAB) deepens, and then the burial in the Alpine foreland during the Cenozoic (One-rift model).
The temperatures are caused by two rifting events during the Early–Middle Jurassic (Alpine Tethys rifting; 201–169 Ma) and the Late Jurassic–Early Cretaceous (Vocontian–Valaisan rifting; 150–129 Ma), followed by thermal relaxation and burial in the Alpine foreland during the Cenozoic (Two-rifts model).
The model calculates for each tectonic scenario the evolution of the temperatures in a stratigraphic column according to the reconstructed burial history. The predicted maximum temperatures are then compared to the Tmax measured at a given depth. The No-rift model assumes a thermally equilibrated post-Variscan European lithosphere characterised by crustal thickness of 30 km and a mantle lithosphere of 90 km (e.g. Mouthereau et al., 2021). For the second and third scenarios accounting for lithospheric thinning, we tested thickness variations ranging from 30 to 8 km, and from 90 to 15 km, for the European crust and mantle lithosphere, respectively. As the margin is inverted during the Cenozoic, crustal and mantle thicknesses are designed to progressively increase to reach their initial pre-extensional values.
In all models, one of the major unknowns is the thickness of sediments (mainly Cenozoic), on top of the sections that have been removed by erosion. In the Barles half window (Fig. 1b), partially reset AFT (apatite fission track) ages documented in Miocene marine molasses reveal maximum burial depths of 3–4 km (Schwartz et al., 2017), an estimate that includes the thickness of the overlying nappe. Further to the SW, beneath the Digne Nappe, the thickness of the Mio-Pliocene series is constrained by the Mirabeau well to 2 km (Fig. 1b, see Graham et al., 2012). According to other thermochronological data obtained in Paleogene sediments in the vicinity of DEV, CLN and SLC sections and farther to the east (Labaume et al., 2008; Jourdan et al., 2013; Schwartz et al., 2017), the domain ranging between fully and partially reset AFT ages defines a region where sediments were heated between 90 and 120 ∘C (Fig. 1b). We therefore infer that a maximum of 3 km of Cenozoic sediments have been eroded at the Digne thrust front (Fig. 1b). In addition, we have also evaluated the amount of missing Cretaceous strata in DEV, SLC and CLN sections based on the surrounding areas where they are preserved. Because all the sections are detached in the Upper Triassic evaporites, which were also involved in salt tectonics since the Early Jurassic (e.g. Célini et al., 2020), it is difficult to estimate their original thickness. We thus assume for every section a reasonable initial thickness of 100 m for the Upper Triassic evaporites. A thickness of 100 m of Lower Triassic sandstones and 50 m of Middle Triassic limestones have been considered based on the thickness exposed in a few location of the SW Alps, including the Lower and Middle Triassic exposed north of Barles in Verdaches (e.g. Haccard et al., 1989).
Physical and thermal properties of the rocks adopted in our models are presented in Table 1. These parameters have been chosen to reproduce the lithologies documented in the sedimentary cover (sandstone, limestone, marls, etc.) and assuming a continental basement with a homogeneous granitic composition. The temperature at the base of the conductive continental lithosphere is fixed at 1333 ∘C (e.g. Mouthereau et al., 2021).
4.1 RSCM temperatures
The RSCM temperatures obtained along the six sections are presented in Fig. 3a (see also details in the Supplement File 1). We systematically observed two temperature trends separated by an abrupt shift of 50–100 ∘C (peak temperature drops in Fig. 3b). In the deeper domain, Tmax measured in Early–Middle Jurassic deposits at reconstructed burial depths between 2 and 4 km range between 200 and 340 ∘C, except for the CAS section (Fig. 3a). In contrast, upper successions of the Upper Jurassic and Cretaceous post-rift strata and the syn-orogenic deposits show Tmax below 150 ∘C (Fig. 3). It is worth noting that the 100 ∘C Tmax drop in section DEV occurs over a few tens of metres, corresponding to a sharp transition in the Middle–Upper Jurassic interval (Fig. 3a). Along the southern CAS section, located in the Castellane Arc, the Tmax does not exceed 170 ∘C at the base of the section. Temperatures from Middle Jurassic series located farther to the east in the Embrun half window range between 300 and 330 ∘C (Fig. 1b). Samples in the Jurassic and Eocene successions from the E-U nappes that overthrust the Digne Nappe (Fig. 1d) yield in contrast, notably lower Tmax between 190 and 225 ∘C (Fig. 3c).
4.2 Evidence for rift-related thermal event recorded at the Digne frontal thrust
The Tmax measured in the uppermost samples of the stratigraphic sections are in agreement with AFT ages from the Eocene strata (CAS, DGN), which show partially reset ages and thus temperatures below 120 ∘C (Fig. 1b; Labaume et al., 2008; Jourdan et al., 2013; Schwartz et al., 2017). Assuming a postextension thermal gradient of 30 ∘C km−1, in line with the upper bounds of published gradients in the SW Alps (e.g. Bigot-Cormier et al., 2006; Valla et al., 2011), Tmax of 100–150 ∘C found in the upper parts of the studied sections are likely to reflect burial in the Alpine foreland. However, a similar burial with the same geothermal gradient fails to explain the high Tmax up to 300–330 ∘C found in deeper Early–Middle Jurassic strata (DEV, SLC, CSN, DGN, CLN sections) as they would imply 6–7 km of foreland sediments at the thrust front and the reset of all AFT ages. In addition, the abrupt ∼ 100 ∘C decrease of RSCM temperatures across the tectonic contact between the Digne Nappe and the E-U nappes (Fig. 3c) suggests that the emplacement of the E-U nappes of the Alpine accretionary wedge is not responsible for the high Tmax observed in the Digne Nappe. If it was the case, we would expect continuously decreasing temperatures across the contact. It is more likely that these higher temperatures in the Digne Nappe represent an older and higher grade thermal event, which produced temperatures too high to be reset by the subsequent Alpine burial. A notable exception is the CAS section in which Tmax are mainly below 150 ∘C and could therefore represent burial in the Alpine foreland only.
4.3 Modelling results
The comparison between the temperatures derived from RSCM analysis and temperatures predicted for the different scenarios based on TemisFlow® 1D modelling is presented in Fig. 4. To quantitatively evaluate our results, we calculated the root mean square (rms) data misfit error between model and observations (Fig. 4). From burial histories modelling we obtained maximum temperatures and geothermal gradients in the stratigraphic columns, shown in Figs. 5 and 6 for the third model only (Two-rifts model), which best fits the measured RSCM temperatures. Refer to the Supplement files for burial histories and geothermal gradients obtained for the two other scenarios (No-rift and One-rift models).
In the first No-rift model, the Tmax are reached during syn-orogenic burial in the Alpine foreland. The fit is good for the uppermost samples but the model fails to reproduce the observed Tmax above 200 ∘C measured in deeper samples (rms ranging from 20 to 77 ∘C) (Fig. 4 and Supplement File 2). The only exception is the CAS section where the sample shows Tmax distinctively colder (Figs. 3 and 4). For the second One-rift model that incorporates crustal thinning to 8-10 km and shallowing of the LAB from 120 to 25 km during the Early–Middle Jurassic, the fit is noticeably better (rms ranging from 17 to 53 ∘C) (Fig. 4) for the deeper samples with higher temperatures (Fig. 4 and Supplement File 3). This is caused by the increase of the crustal geothermal gradient from 70 to more than 90 ∘C km−1 that results from lithosphere thinning (Supplement File 4). The third Two-rifts model (Fig. 5), which includes the superimposition of two rifting events in a few tens of millions of years, presents a much better fit of the temperatures both for the shallower and deeper samples with noticeably lower rms in the 13–32 ∘C range (Fig. 4).
Burial histories obtained from the Two-rifts model show that the deepest sediments record Tmax between 230 and 330 ∘C during the Early Cretaceous (∼ 130 Ma, Fig. 5). As a result of the lithospheric thinning, crustal geothermal gradients increased from 50 to 60 ∘C km−1 during the Early–Middle Jurassic to 80–90 ∘C km−1 during the Early Cretaceous (Fig. 6). The cumulated thermal effect of the Jurassic and Early Cretaceous rifting is required to fit the RSCM data, especially to reproduce the temperatures below 2 km (Fig. 4). The last rifting event is followed by thermal relaxation as geothermal gradients return to their initial value of 30 ∘C km−1 due to deepening of the LAB 1333 ∘C isotherm from the Late Cretaceous. Most of the reconstructed Tmax in the stratigraphic sections agree with the hypothesis of 3 km of eroded Cenozoic deposits. The only exception is the CSN section, which has required 4 km of burial in the foreland to fit the Tmax of the upper part of the section. This value agrees with a thermochronological study on Eocene–Oligocene deposits indicating that these syn-orogenic deposits can have reached around 4 km in that location of the Alpine foreland (Fig. 1b, Labaume et al., 2008). The temperatures of the colder CAS section can be accounted for by any of our scenarios with relatively low rms values (Fig. 4). Although this section is noticeably thinner that the others, the burial history of CAS is characteristic of the Dauphinois palaeogeographic domain (Figs. 5f and 6f), as shown by the continuous subsidence from the Early Jurassic to the Early Cretaceous. We infer that the temperature evolution of the CAS section is consistent with the Two-rifts model.
It should be noted that the evolution of geothermal gradients as a function of burial history locally reveals greater gradients for model cells located upwards (Fig. 6). This reflects the variability of thermal conductivities in sedimentary facies resulting in contrasting local geothermal gradients. These numerical simulations also reveal that the higher thermal gradients computed in the upper part of the section are maintained for a longer period of time, i.e. before gradients reduce to 30 ∘C km−1 during the Cenozoic (Fig. 6).
5.1 Tmax explained by lithospheric thinning
In our preferred Two-rifts scenario, higher Tmax observed in the Digne Nappe are reached during the second phase of lithospheric thinning of the European margin during the Early Cretaceous, when the overburden is 3–4 km thick and geothermal gradients in the upper crust reached 80–90 ∘C km−1 (Fig. 6). Only a limited combination of crustal thicknesses of 8–10 km and lithospheric mantle thicknesses of 10–15 km (Fig. 5) can reproduce the RSCM data. This scenario implies a significant thinning of the European lithosphere from 120 to 20–25 km resulting from a protracted period of stretching lasting from the Early–Middle Jurassic (201–169 Ma) to the Late Jurassic–Early Cretaceous (150–129 Ma). The total crustal stretching deduced from our models (β-factor) is 3–3.75 and reaches 6–9 for the lithospheric mantle, thus suggesting a depth-dependent stretching mechanism. We note that the crustal stretching factor of 3–3.75 fits well with the crustal thicknesses typically found at the transition between necking and hyperthin domains of magma-poor rifted margins (e.g. Tugend et al., 2015). However, our best Two-rifts model does not require mantle exhumation.
Thermomechanical models of collisional orogens show that high gradients of 80 ∘C km−1 inherited from the rift evolution are preferentially preserved in the less deformed retro-wedge side located on the upper plate (e.g. Jourdon et al., 2019; Ternois et al., 2021). Our study shows that this may also occur in the lower plate at the front of orogenic wedges where crustal thickening is not sufficient to overprint the rift-related thermal peak.
5.2 Tectonic reconstruction of Early Cretaceous rift in the SW Alps
Tectonic and palaeogeographic reconstructions of the SW Alps (Fig. 7a) reveals that Jurassic–Early Cretaceous successions of the Digne Nappe were originally located to the East of the Vocontian Domain (Beltrando et al., 2012; Dumont et al., 2012; Angrand and Mouthereau, 2021; Lemoine et al., 1986), in the continuation of the Valaisan Domain and separated from it by a NW–SE transfer zone (Lemoine et al., 1989). The existence of this transfer zone is justified by the large extension accommodated in the Valaisan Domain as indicated by mantle exhumation and magmatism that strongly contrasts with the lower extension in the area of the Vocontian Domain and the Digne Nappe where a remaining crustal thickness of 10 km is proposed (Figs. 5 and 7b). The transfer zone is aligned in the direction of extension along the eastern borders of the Argentera and Pelvoux massifs (Lemoine et al., 1989). The lack of continuity of the Valaisan Domain towards the SW also points to this.
Numerical models of propagating rifts and spreading ridges show that such transitional domain can localise extension for tens of millions of years before the rift actually propagates into the continent (Jourdon et al., 2020). The different duration of rifting between Vocontian and Valaisan domains provides a good analogue of such 3D architecture of extensional systems. The end of rifting in the Vocontian Domain and the Digne Nappe area is indeed constrained in our model to be around 130 Ma, but extension in the Valaisan Domain is suggested to have persisted until 110–90 Ma. Rift propagators are also sites of asthenospheric flow oriented parallel to the rift axis (Mondy et al., 2018). In this case of westward propagating rift in the SW Alps, the asthenospheric mantle flow and lithosphere thinning are likely to transfer heat laterally from the Valaisan to the Vocontian domains. Accounting for these three-dimensional thermal effects should potentially reduce the lithospheric stretching needed to fit the data, and this is yet to be evaluated.
In the reconstruction of Fig. 7 the flysch deposits of the E-U nappes are supposed to be originally deposited over the Alpine Tethys, the Briançonnais and the Valaisan domains, which corresponds to the current position of the internal zones. The tectonic thickening of the E-U nappes reaches a maximum in the east of the Embrun half window (Fig. 1b), where Tmax measured in the E-U nappes and the Digne Nappe are very close (Fig. 3c). These temperatures thus can be explained by a nappe stacking of ca. 10 km when approaching the internal zones under a normal gradient of 30 ∘C km−1. The Tmax difference observed at the NW front of the E-U nappes (Figs. 1b and 3c), however, reflects the overthrusting of the internally derived E-U nappes and also requires heating of the Jurassic successions before the emplacement of the E-U nappes. Based on our analysis of the Digne main thrust, those mid-crustal temperatures may reflect pre-Alpine heating, and temperatures inherited from the same Early Cretaceous thermal event. This implies that the thermal anomaly would not only be restricted to the Digne thrust front but must be of regional importance extending farther to the east (Fig. 7).
5.3 Rift-related metamorphism in the SW Alps?
The significant thinning of the lithospheric mantle is the dominant factor explaining the thermal (Fig. 5) and geothermal (Fig. 6) structures reached during the Early Cretaceous. The high geothermal gradients of 80–90 ∘C km−1 inferred from the modelling (Fig. 6) have been recognised in other inverted rift basins of Europe. This is the case for the Early Cretaceous Pyrenean rift system (Vacherat et al., 2014; Hart et al., 2017; Saspiturry et al., 2020; Clerc and Lagabrielle, 2014; Clerc et al., 2015) where such geothermal gradients are accompanied by high-temperature metamorphism, hyperextension and mantle exhumation (e.g. Ducoux et al., 2021). Laterally, to the west it leads to continental break-up and oceanic spreading in the Bay of Biscay. Similarly, high geothermal gradients have also been reconstructed in the Cameros Basin in the Iberian Range (Rat et al., 2019) where metamorphism and hydrothermalism have been recognised.
Temperatures locally above 300 ∘C found at the front of the Digne Nappe (Figs. 1d and 3) are consistent with previous estimations of the illite crystallinity index (Aprahamian, 1988) and the proportion of chlorites in clay mineral assemblages recognised in the Mesozoic formations of the region (e.g. Artru, 1967; Levert, 1991). They are indicative of diagenesis to weak metamorphism (anchizone). The pressure–temperature conditions for regional greenschist metamorphism are not met in the Digne Nappe at the time of Tmax acquisition due to low lithostatic pressures (0.9–1.2 kbar) and the lack of metamorphic fluids at the base of the nappe. Mineralisation of barite, authigenic quartz and pyrite in the Callovian–Oxfordian shales of the Terres Noires formation (Fig. 1c) are described locally in both the hanging wall and the footwall of the Digne thrust (Guilhaumou et al., 1996). They form mineral concretions from which fluid inclusion in quartz revealed temperatures up to 250 ∘C and pressures of 0.6–0.8 kbar. These local fluids are interpreted as reflecting the maximum burial of the Jurassic black shales acquired during the Middle Cretaceous (Guilhaumou et al., 1996), thus confirming our results. We infer that the groups of homogeneous temperatures found at the base of the sections might have required localised influx of hot fluids to allow an efficient heat transport in the sedimentary cover but did not result in rift-related metamorphism.
The RSCM approach has been applied to 90 CM-rich samples collected along the front of the Digne Nappe, in its autochthonous and in the Embrunais–Ubaye nappes. Palaeotemperatures of about 300 ∘C reported at the front of the SW Alps are close to or even higher than palaeotemperatures reported from the internal domains (e.g. Briançonnais). Basin modelling has been used to test three scenarios (No-rift, One-rift and Two-rifts models) to reproduce the Tmax. The results of numerical modelling reveal that the Two-rifts model provides the best fit for the observed temperatures. These mid-crustal temperatures are interpreted to be inherited from a long-lasting lithospheric stretching process between Europe and Adria–Iberia. Tmax were reached during the Early Cretaceous (∼ 130 Ma) corresponding to geothermal gradients of 80–90 ∘C km−1 that are not related to crustal thickening during orogeny. Our study argues that the recognition of collisional thermal events in accretionary prisms may be elusive without a careful analysis of the pre-orogenic thermal evolution of the accreted units. Tmax reconstructed in orogens might therefore not illustrate nappe stacking or maximum syn-orogenic burial in the foreland, but instead could represent pre-orogenic thermal conditions. This can lead to overestimating both orogenic thickening and horizontal displacement in mountain belts. This issue is likely to be more significant in older orogenic systems where details of the original structural relationships are lacking. In the case of the Alps, the identification of an Early Cretaceous thermal event introduces new constraints on the palaeogeographic and kinematic reconstruction of the Alpine Tethys, and on the rift architecture.
All the data used in this manuscript are available in the Supplement and can be provided by the corresponding authors upon request.
The supplement related to this article is available online at: https://doi.org/10.5194/se-14-1-2023-supplement.
NC realised the investigation, conceptualisation, visualisation, formal analysis and the writing of the original draft. FM realised the investigation, conceptualisation and correction of the manuscript, and he acquired funding for the study. AL realised the investigation, formal analysis, and acquisition of resources and funding for the study. CG provided the software for modelling and participated in resource acquisition and reviewing of the manuscript. JPC realised the investigation and editing of the manuscript and participated in the funding acquisition.
The contact author has declared that none of the authors has any competing interests.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
We wish to thank Yann Rolland and two anonymous referees for their thorough comments. Mary Ford is also thanked for comments on an earlier version of the manuscript. Beicip-Franlab is acknowledged for providing licences for the basin simulator TemisFlow™.
The work has been supported by the Agence Nationale de la Recherche, Carnot Institute ISIFOR and BRGM.
This paper was edited by Stefano Tavani and reviewed by Yann Rolland and two anonymous referees.
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