Lithospheric tear faults or subduction–transform edge propagator (STEP) faults are propagating strike-slip faults that accommodate the differential motion between the retreating subduction zone and the overriding plate (Govers and Wortel, 2005). Because of the relative motion between back-arcs and surrounding plates, they are also propagating strike-slip faults defined by a sharp contrast in crustal thickness. As noted by Govers and Wortel (2005), such oblique fault boundaries do not necessarily form proper transform plate boundaries, but instead form broad zones of distributed deformation, accommodating differential trench-parallel extension, strike-slip motion, and rotation. In case the lithospheric tear propagates within the continent–ocean transition, a narrow continental margin forms highly oblique to the direction of back-arc extension. This is documented, for instance, in the Caribbean, along the transcurrent Caribbean–South American plate boundary (Pindell and Kennan, 2009) or on the margin of the South Orkney Microcontinent, along the Scotia–Antarctic plate boundary (Dalziel et al., 2013). Despite the large-scale kinematic picture being relatively well understood, there are only a few places on Earth where continental crustal deformation associated with a slab edge continental rift system can be studied both on land and offshore.

Here, we focus on the eastern Betic Cordillera, which constitutes a rifted margin defined by decreasing crustal thickness from > 35 to 20 km onshore (Diaz et al., 2016), thinning offshore to 16–6 km in the eastern Alboran arc to the back-arc region (Booth-Rea et al., 2018; Gómez de la Peña, 2020a) (Figs. 1 and 2). This region is seen to develop above a E–W-trending STEP fault at the boundary between the Alboran basin and the Iberian paleomargin (Badji et al., 2014; Gallais et al., 2013; Jolivet et al., 2021a; Mancilla et al., 2015a). The tectonic expression of the strike-slip deformation during E–W-directed crustal extension above the lithospheric tear is, however, controversial. On the one hand, low-angle ductile extensional detachments with a top-to-the-west sense of shear are the main features accommodating deformation in the overriding plate. Yet, A-type metamorphic domes in the lower crust, elongated parallel to the E–W direction (Fig. 1) and formed during the early Miocene, are viewed to express the transtensional deformation at the tip of propagating tear (Le Pourhiet et al., 2012). On the other hand, E–W-directed transfer strike-slip faulting is interpreted as a late (post-middle Miocene) brittle deformation feature associated with differential E–W crustal extension between the metamorphic domes in the eastern Betics (Alpujarras fault zone; Sanz de Galdeano and Vera, 1992; Sanz de Galdeano et al., 1985; Martínez-Martínez et al., 2006) and in the western Betics (Torcal fault zone; Barcos et al., 2015) unrelated to ductile deformation (Fig. 1). In line with the latter interpretation, the dextral motion these transfer faults accommodate is assumed to be modest, reflecting a recent post-8 Ma kinematic change that accompanies the stalling of westward slab rollback, the onset of tectonic inversion in the Gibraltar Arc (Do Couto et al., 2014; d'Acremont et al., 2020; Jolivet et al., 2021a; Martínez-García et al., 2017), and progressive slab tearing and delamination of the lithospheric mantle from the eastern to the central Betics (Martínez-Martínez et al., 2006; Mancilla et al., 2015a; García-Castellanos and Villaseñor, 2012; Spakman et al., 2018). Note that in a recent study the dextral displacement since 9 Ma has been estimated to more than 100 km along the Torcal Fault (Crespo-Blanc et al., 2016).

The lack of structural temporal constraints and quantification of belt-parallel motion along these faults indicates, however, that we do not yet fully understand their link with the long-term evolution of slab tearing and margin formation. For instance, the current deformation patterns in the central Betics, where metamorphic domes are present, brings evidence that both strike-slip faulting and extension operate synchronously (Martínez-Martínez et al., 2006). This is shown by the west-directed GPS velocities increasing westwards indicating ongoing extension, and the west-directed displacements increasing from north to south, towards the Alboran domain, revealing right-lateral shear (Fig. 2). This, together with evidence for present-day 4.5 mm yr-1 westward displacement and rotations in the western Betics and Rif, reveals that the westward slab rollback is likely to be still ongoing (Fadil et al., 2006; Gonzalez-Castillo et al., 2015). The current transtensional deformation across the Betic Cordillera is consistent with the current stress regime defined by extension direction highly oblique (max. 20∘) to the Betic structural trend (or 70∘ spanned by the direction of extension and normal of the rift trend).

Right-lateral transtensional deformation in the Betics agrees with the extrusion model of the Alboran basin towards the Gibraltar Arc to the west (Borque et al., 2019; Palano et al., 2015) caused by indentation by the east Alboran domain likely enhanced by resistance slab dragging (Spakman et al., 2018). In the east, the extrusion is accommodated by left-lateral strike-slip displacement along the Eastern Betic Shear Zone (EBSZ; Borque et al., 2019), shaped by the Carboneras Fault (CF) and Palomares Fault (PF), which separates the extrusion domain, where extension and transtension is prevailing, from the Águilas Arc, where N–S indentation is well documented (Ercilla et al., 2022). In this region, this fault extends offshore, across the Alboran Sea, in the larger Trans-Alboran Shear Zone (De Larouzière et al., 1988; Stich et al., 2006) moving at ∼ 4 mm yr-1, equivalent to the regional 5 mm yr-1 NW-directed convergence between Africa (Nubia) and Europe (Fig. 2; Echeverria et al., 2013; Koulali et al., 2011; Nocquet, 2012; Palano et al., 2015, 2013; Vernant et al., 2010). Here, we hypothesize that the present-day oblique extension pattern has been at play since the Miocene and explains the formation of the narrow Alboran rifted margin.

Only recently high-resolution 3D numerical models have been able to predict the deep structure of oblique rift domains. These models can be used as a guide to re-evaluate the evolution of the Betics. Three-dimensional models by Jourdon et al. (2021) predict that oblique extension results in narrow rifted margins, strike-slip faults, and corridors coupled with subsident pull-apart basins, normal faults, and block rotations (Fig. 3). The recognition of block rotation in the Betic Arc (Crespo-Blanc et al., 2016; Platzman, 1992), strike-slip fault zones (Fig. 1) and NW–SE normal faulting, which defines extension direction highly oblique to the margin (Galindo-Zaldivar et al., 2003; Figs. 1 and 2), support this view. The simulations also show that the deeper ductile crust experiences thinning (vertical flattening) and stretching perpendicular to the strike of the margin in accordance with stretching lineations parallel to the metamorphic domes and low-angle detachments (Fig. 3). Other types of 3D numerical experiments show that sediment loading of strike-slip faults can result in asymmetric flexural basins with apparent normal fault throw (Neuharth et al., 2021) that can be mistakenly interpreted as resulting from orthogonal extension. Asymmetric basins are indeed intriguing characteristics of intramontane basins in the Betics (Rodríguez-Fernández et al., 2012; Augier et al., 2013; Do Couto et al., 2014; Giaconia et al., 2014). Although primarily found associated with divergent plate boundaries, e.g. in the Gulf of California (Fossen et al., 2013; Fossen and Tikoff, 1998), highly oblique extension is also documented in active transform regions along the San Andreas Fault (Teyssier and Tikoff, 1998) or the North Anatolian Fault in the Sea of Marmara (Okay et al., 2004). A detailed analysis of highly oblique rifting deformation in the Gulf of California recognizes similar tectonic elements to those for the Betics, such as extensional detachment systems orthogonal to the divergence and upper crustal folds trending parallel to the divergence (Fossen et al., 2013).

However, several tectonic features need further discussion. First, the relevance of strike-slip faulting in the past is debatable as only a few occurrences of crustal-scale strike-slip faults are mapped (Fig. 1). Second, the detail of the temporal and spatial relationships between the formation of the oblique–transform margin and STEP faulting remain elusive. We here review the temporal and spatial evolution of Neogene intramontane sedimentary basins and related brittle deformation in the eastern Betics. In addition, we exploit offshore seismic reflection lines to propose a new crustal-scale section across the oblique margin. Based on these constraints we present a tectonic scenario for the formation of the high-obliquity rifted margin controlled by STEP faulting.

The most prominent extensional features in the eastern Betics are (1) the E–W elongated ranges that formed metamorphic domes with foliations bearing prominent E–W stretching lineations, for instance, in the Nevado-Filábride Complex (Fig. 5; e.g. Sierra de los Filabres, Sierra Nevada, and the Sierra de las Estancias) and Serravallian-Tortonian sedimentary basins (Tabernas-Sorbas, Alpujarras, Almanzora and Huércal-Overa basins), and (2) the NNW–SSE and NW–SE normal fault systems and basins oblique to the domes such as the NW–SE-trending Guadix-Baza and Alhabia basins (Galindo-Zaldivar et al., 2003; Martínez-Martínez and Azañón, 1997) (Fig. 5). They are described as asymmetric half grabens (Do Couto et al., 2014; Martínez-Martos et al., 2017; Pedrera et al., 2010, 2009) formed during the upper Serravallian–early Tortonian (Augier et al., 2005b, 2013; Meijninger and Vissers, 2006). Several of these NW–SE faults are active and cut across the metamorphic domes and the sedimentary basins (Augier et al., 2005a; Booth-Rea et al., 2004a; Giaconia et al., 2012; Montenat and d'Estevou, 1999).

In addition to these structures, there are E–W right-lateral strike-slip fault zones and parallel depressions, like the Alpujarras fault zone between the Sierra de Gádor and the Sierra Nevada and the Almanzora fault zone between the Sierra de los Filabres and Sierra de las Estancias (Fig. 5). The left-lateral Carboneras and Palomares fault system (Reicherter and Hübscher, 2006; Scotney et al., 2000) marks the tectonic limit with the Cabo de Gata volcanic province (Fig. 5).

The domes are extension-related features interpreted either as (1) E–W metamorphic domes resulting from the exhumation in the footwall of a regional W-directed extensional low-angle detachments, later folded during post-Tortonian N–S contraction (Martínez-Martínez and Azañón, 1997; Martínez-Martínez et al., 2002, 2004) or (2) Miocene metamorphic domes formed by constrictional ductile strain regime accompanying W-directed stretching of the Alboran domain and trench retreat, with limited overprint by the Tortonian contraction ca. 8 Ma (Augier et al., 2013, 2005c b; Galindo-Zaldivar et al., 2015; Jolivet et al., 2021b; Martínez-Martínez et al., 2002). Low-temperature constraints from the Nevado-Filábride and Alpujarride complexes confirm the W-directed exhumation of the basement that occurred progressively from the Sierra de los Filabres at ∼ 13–11 Ma (Serravallian) in the east to the Sierra Nevada at 8–6 Ma (Late Tortonian–Messinian) in the west (Clark and Dempster, 2009; Janowski et al., 2017; Johnson et al., 1997; Platt et al., 2005; Reinhardt et al., 2007; Vázquez et al., 2011).

Tectonic models for the formation of Neogene intramontane sedimentary basins vary depending on the prevailing tectonic regime. E–W-directed basins have been early described as pull-apart basins (e.g. Alpujarras fault zone; Sanz de Galdeano et al., 1985). Structural analyses then led to reinterpret these structures as transfer zones resulting from differential extension between exhuming core complexes (and detachment systems) since the Serravallian (13–11 Ma) later refolded during Tortonian (9–8 Ma) compression in the eastern Betics while extension is still active in the central Betics (Martínez-Martínez et al., 2006). Other authors proposed that NE–SW extension lasted until 7.5–7 Ma in the eastern Betics (Booth-Rea et al., 2004b; Giaconia et al., 2014).

In support to the compressional stress regime in the eastern Betics, Martiìnez-Martos et al. (2017) interpreted the E–W depressions as being related to the tectonic reactivation of crustal weakness zone as dextral strike-slip faults in an anticlockwise rotation, accommodating part of the N–S shortening. There is evidence that at the end of the Tortonian a regional uplift occurred, raising the remnants of late Tortonian marine platform, 7.2 Ma in age, to 1600 m above sea level in the Sierra de Gádor (Braga et al., 2003; Janowski et al., 2017), coincidently with the onset of contraction in the Sierra Alhamilla and Sierra de los Filabres (e.g. Do Couto et al., 2014), in the Alboran domain (e.g. Martínez-García et al., 2017), and on the margins of the eastern Betic (Giaconia et al., 2013, 2015). In addition to shortening, this recent uplift may reflect deep-mantle mechanisms like slab tearing or delamination (e.g. Duggen et al., 2003; García-Castellanos and Villaseñor, 2012; Mancilla et al., 2015a).

Based on the prevalence in some E–W-trending basins, like the Huércal-Overa basin, of E–W-trending normal faults, these basins have alternatively been interpreted as resulting from late exhumation stage of the domes, possibly as soon as the Serravallian but mostly after the early Tortonian (syn-sedimentary faulting) (Augier et al., 2013, 2005b; Meijninger and Vissers, 2006). The NW–SE or NNW–SSE sedimentary basins (Guadix, Baza, Alhabia; Fig. 5), in contrast, are extensional basins formed parallel to the direction of the regional compression (Sanz de Galdeano and Vera, 1992; De Larouzière et al., 1988). E–W strike-slip fault zones, aligned in the direction of the domes, and NW–SE normal faulting patterns are both key features consistent with predictions from models of oblique extension at transform margin (Fig. 3). Yet, based on existing structural and tectonic syntheses a clear temporal relationship between E–W ductile stretching in the domes and transcurrent deformation is not established (Fig. 5).

The stratigraphic architecture and depositional evolution of Tortonian intramontane basins provides first-order information on the distribution of crustal thinning. Among the oldest sediments deposited unconformably on the Paleozoic–Triassic basement are the red alluvial conglomerates and deltaic series dated from the Serravallian to the Lower Tortonian (Fig. 6a). They are thicker and well exposed on the flanks of the Almanzora basin and on the northern Huércal-Overa basin (HOB), compared to the Alpujarras Corridor (AC) and Tabernas basin (TB) (Figs. 6 and 7a; Augier et al., 2013; Pedrera et al., 2010, 2007; Poisson et al., 1996). In the east of the Sorbas basin, it should be noted that Langhian–Serravallian deposits and perhaps sediments as old as Burdigalian have been locally reported (Giaconia et al., 2014).

Paleogeographic reconstructions indicate that these Serravallian to Lower Tortonian sediments were deposited on a large emerged domain, stretching from Huércal-Overa to Granada in the west and Tabernas to the south (Braga et al., 2003). Sourced from the Nevado-Filábride metamorphic complex (Hodgson and Haughton, 2004; Kleverlaan, 1989; Meijninger and Vissers, 2006; Pedrera et al., 2010, 2007; Pickering et al., 2001; Weijermars et al., 1985), these deposits mark the onset of surface exhumation of the Sierra de las Estancias and Sierra de los Filabres.

During this initial stage, HOB is the most subsident basin (Figs. 6b, 7a, b), accumulating sediments at rates of 400 m Myr-1 while rates are 140–180 m Myr-1 in the Tabernas basin (Fig. 6b) (Augier, 2004). Higher subsidence in the HOB, which also started earlier than in other basins, suggests extension occurred originally to the north associated with the exhumation of the Sierra de Las Estancias. Basal continental conglomerates are overlain by grey coarse-grained Tortonian sandstones found occasionally, e.g. in the Almanzora basin, intercalated with marine marls (Fig. 6a). They are topped by mid-Tortonian bioclastic calcarenite and coral reefs (Braga et al., 2003; Martin et al., 1989; Pedrera et al., 2007).

During the same interval, TB recorded the deposition of 300 to 400 m of coarse- to medium-grained deltaic marine clastics unconformably overlying the lowermost red series (Fig. 6a). These sediments pass upwards, e.g. in TB, to deeper marine 1200 m thick turbiditic and marls series intercalated with regional-scale mega-beds, revealing the onset of rapid tectonic subsidence (Haughton, 1994; Kleverlaan, 1989, 1987; Pickering et al., 2001; Weijermars et al., 1985). Details of depositional architecture of the Tortonian suggest that part of this subsidence evolution was controlled by E–W dextral strike-slip faults (Haughton, 2000; Baudouy et al., 2021) under transtensional strain.

The transition from continental to deep marine sedimentary environments (water depth of 400–600 m according to Poisson et al., 1999) witnesses the rapid rift-related tectonic subsidence achieved during the upper Tortonian times (∼ 9 Ma; Figs. 6 and 7c) (Augier et al., 2005b; Montenat and Ott d'Estevou, 1992; Weijermars et al., 1985). At around 8 Ma, accumulation rates drop by a factor of two to 200 m Myr-1 in HOB and 70 m Myr-1 in TB, revealing a marked reduction in subsidence. Subsidence then became negative as basement uplifted from around 7 Ma (Figs. 6b and 7d) in both TB and HOB.

The geometry of the Almanzora (Pedrera et al., 2009), Sorbas (e.g. Do Couto et al., 2014) and Huércal-Overa basins (Pedrera et al., 2010) inferred from gravity measurements indicate that these basins are asymmetrical and deepening southwards. This sediment infill pattern recalls the formation of asymmetrical basins predicted by numerical models of flexural strike-slip basins (Neuharth et al., 2021). According to this model, the asymmetry observed should reflect the development of strike-slip basins loaded by sediments originating from the north. In addition, a larger subsidence in HOB is an indication of abrupt crustal thinning to the south of Sierra de las Estancias where the crustal thickness is the largest (Fig. 2). Therefore, at least the Serravallian–Tortonian infill patterns agree with oblique extension.

Figure 8 presents a compilation of 112 fault slip data inversions previously analysed in the eastern Betics combined with new measurements conducted in the Alpujarras Corridor and in the Tabernas basin (Table S1 in the Supplement). Most faults are syn-Tortonian or cut through the Tortonian. This compilation emphasizes a regional trend of σ3 stress axes oriented NNE–SSW (north 0∘ E) with subordinate σ3 oriented E–W. In detail, this well-defined regional horizontal extension reflects a combination of pure normal faulting regime (σ2 horizontal and oriented NW–SE or WNW–ESE; 73 % of stress tensors) and strike-slip faulting regime (σ2 vertical to steeply dipping and σ1 horizontal and striking NNW–SSE; 27 % of stress tensors). N–S to NW–SE compression is also reported in the HOB associated with incipient syn-form and depocentre, which is dated to the lower Tortonian coeval with the prominent E–W and WSW–ENE extension (e.g. Pedrera et al., 2010).

We describe below, based on a selection of outcrops in the vicinity of the contact between Tortonian basins and major metamorphic domes, the expression of E–W and NW–SE extensional faulting in the field. We then discuss how they are linked to the regional stress regimes.

In Tortonian intramontane basins, one of the main set of faults is represented by E–W-directed faults, including ENE–WSW to ESE-WNW sets. North of the Alpujarras Corridor (AC), 3 km to the NE of Canjáyar, the contact between the basal Tortonian conglomerates and the series of Alpujarride complex is exposed in the Rambla de Tices. It is shaped by a 2 m thick fault zone (Fig. 9a, b) striking north 100∘ E, which has a normal sense of slip with a right-lateral strike-slip component (Fig. 9c). It consists of cataclastic breccias and sheared blocks (boudins) of the host rocks (Fig. 9d). This major fault is found along the 65 km long Alpujarras fault zone described by Martínez-Martínez (2006) as a major strike-slip dextral transfer zone south of the Sierra Nevada that accommodates both W–SW extension and dextral movement. It is mechanically consistent with NE–SW and ENE–WSW extension under a strike-slip regime as resolved nearby along the same fault system (Martínez-Martínez, 2006). Figure 9 indicates the fault is parallel to the basal Tortonian series but cuts across the Alpujarride complex. In the HOB, on the southern flank of the Sierra Limaria (Fig. 8), the unconformity between the lower Tortonian red conglomerates and the Alpujarride units (Rambla de Cordoba, 2 km NW of Arboleas, Figs. S1a, b) is found reactivated as a normal fault with a dextral shear component.

To the north of TB, a large morphological surface presents a rare exposure of the micaschist basement of the Nevado-Filábride (NF) complex allowing the study of deformation on the southern flank of the Sierra de los Filabres (Fig. 10). The deformed NF series shapes a kilometric-size antiform with an axial planar surface dipping towards the north. The steeply dipping cleavages directed NE–SW on its southern flank are deformed by numerous dextral shear zones with lengths ranging from 100 m to less than 5 m (Fig. 10b, c). In addition to isoclinal folds parallel to the main foliation that are clearly associated with an early stage of ductile E–W stretching, we recognize steeply dipping metric-size open to tight folds inclined to the NE close to the strike-slip shear zones (Fig. 10d). To the south, Tortonian conglomerates are unconformably overlying the folded NF foliation. This stratigraphic relationships and the average low dip of Tortonian strata (20∘ to the SE) indicate that strike-slip deformation occurred before the deposition of Tortonian conglomerates and after the tilting of the NF foliation (see cross section in Fig. 10a). This argues that the transition from HP metamorphism (Burdigalian–Langhian) in the NF (Platt et al., 2006) to W-directed ductile crustal thinning and right-lateral strike-slip faulting occurred before the Tortonian, most likely around the Serravallian at 12–13 Ma. This interval is considered to mark the transition from ductile to brittle extension in the region (e.g. Augier et al., 2013). Because strike-slip faulting postdates folding of the NF foliation and is consistent with WSW–ENE oblique extension, we suggest that the Sierra de los Filabres metamorphic dome formed in a transtensional strain regime. This hypothesis conforms with prediction of transtension at the tip of the STEP fault (Le Pourhiet et al., 2012) and with model of oblique extension (see Fig. 3).

A second set is represented by NW–SE-directed normal faults (Fig. 8). They are found, for instance, bordering the NE part of Alhabia basin, where they cut across the basement and interrupt the westward continuity of the southern flank of the Sierra de los Filabres. One major fault zone of this system is well exposed in the Arroyo del Verdelecho, 7 km to the west of Tabernas, on the eastern border of the Alhabia basin (Figs. 11 and S2). From a regional point of view, this large NW–SE fault zone controls the deepening of the Tortonian basin and the position of Pliocene depocentre in its hanging wall towards the west. NW–SE normal faults also cut across the lower Tortonian conglomerates in the hanging wall, but their throw diminishes upward in the upper Tortonian margin sediments, suggesting fault activity during the late Tortonian (Fig. 11). One major fault zone is outlined by cataclastic breccias made of marbles originating from the exhumed Alpujarride complex in the Sierra de los Filabres (Fig. S2).

South of HOB (south of Arboleas), NW–SE faults are seen cutting through the late Tortonian sands and marls series, indicating that NE–SW extension is at least Tortonian (Fig. S1c, d).

Both fault slip data and our own observations argue for a regional pre-Tortonian and syn-early Tortonian NNE–SSW-directed extension. This direction of extension is also found associated with less well-developed strike-slip regimes (Fig. 8). It is consistent with the D1–D2 phase of brittle deformation found in HOB (Augier et al., 2013). The fact that extension and strike-slip regimes occurred synchronously, or overlap rapidly in time, supports the view that they reflect the same large-scale tectonic setting. The reason why strike-slip faulting is less apparent in the field than expected in models in Fig. 3 is likely to reflect the fact that oblique extension is not fully partitioned between normal and strike-slip components and is actually distributed along oblique structures. Moreover, where strike-slip faults are found they are associated with narrow basins or near the contact between the cover and basement but not in the centre of HOB or TB. The NNE–SSW to NW–SE faults appear to postdate the deposition of the early Tortonian red conglomerates and are synchronous with the deposition of marine Tortonian series (Fig. 12). These normal faults currently form half-graben filled with Plio-Quaternary deposits (Guadix, Baza, Alhabia) and are active today. However, the importance of extension-related brittle deformation over brittle compression decreases eastwards. Indeed, a late brittle compressional event oriented roughly N–S is described in the literature as a D3 brittle event (e.g. in HOB) associated with reverse and strike-slip faults (Augier et al., 2013). The post-late-Tortonian shortening is seen as responsible for fold amplification and reverse faulting on the northern limb of Sierra Alhamilla and Sierra de los Filabres and locally in the eastern part of the HOB near the termination of left-lateral strike-slip faulting evolution of the Alhama de Murcia Fault (Fig. 8).

The Carboneras Fault is well imaged north of MSB07 (Fig. 13). It forms a negative crustal-scale flower structure related to left-lateral strike-slip faulting that involves a Moho depth variation between 12 and 9–8 s TWTT after Gómez de la Peña et al. (2018). It separates a thin continental crust to the north (25–20 km; Fig. 2) from the magmatic calc-alkaline arc crust of the EAB with a thickness of 18 km in the south (Booth-Rea et al., 2007, 2018; Gómez de la Peña et al., 2018, 2020a).

Reflection seismic data (Figs. 13, 14, 15) collectively show a stratified crust, corresponding to the sediment cover, down to 2.4–4 s TWTT, which outlines the acoustic basement with high reflectivity (B). Locally, the top basement reflector coincides with erosional palaeo-relief or high angle normal faults bounding basement highs. These faults are oriented mostly NW–SE to NE–SW and cut across the basement. We recognized on seismic images magmatic additions in the continental crust that are shaped by volcanic edifices exposed on the seafloor (e.g. Chella Bank) or slightly buried (Alboran Ridge) outlined by symmetric downlaps and onlaps of sediments. These constructions form topographic highs such as the Chella Bank on the MSB08 line (Fig. 14), the Alboran Ridge on the MSB07 line (Fig. 13), and the Maimonides Ridge on the ESCI-Alb2b line (Fig. 15). All the reflectors corresponding to layers as old as the Tortonian are onlapping against the volcanic ridges confirming that the volcanic activity occurred during middle to late Miocene times, which is shown by Duggen et al. (2008). Some reflectors up to the top Messinian (top M) onlap onto the volcanic ridges, probably as a result of Pliocene uplift.

The stratigraphy offshore, on the continental crustal domain, is defined by the recognition of five seismic stratigraphic units in the Andalucía-A1 well (Jurado and Comas, 1992) labelled I–V from top to base (Figs. 6 and 16) and separated by unconformities. The seismostratigraphic units I to V vary in thickness (Fig. 16), and their architecture is conditioned by the occurrence of basement highs and crustal-scale faults.

Below the Miocene sedimentary filling, the Andalucía-A1 well reveals ∼ 190 m of phyllitic and quartzitic meta-sediments (2.4 to 4 s TWTT below the Alboran basin, Figs. 13 and 14) topped by Langhian to Tortonian marls (top at ∼ 1.6 to 3.4 s TWTT below the Alboran basin) interbedded with Tortonian–Messinian tuffs and basaltic lavas. These units have been correlated in the magmatic arc crust of EAB after Gómez de la Peña et al. (2020b). The older deposits (Unit V) are Langhian–Serravallian in age and consist of clays and marls with intercalated sands and volcano-clastic deposits. The seismic facies of this Unit V are made of moderate-amplitude and low-frequency discontinuous reflections packages (Fig. 16) and are only present in the northern Alboran basin. They are correlated with volcanic series in the EAB (vY3) (Gómez de la Peña et al., 2020b). They pass upward into Serravallian sand–silty clay turbidite (Unit IV) possibly correlated with volcanic series in EAB (vY2 after Gómez de la Peña et al., 2020b). This unit exhibiting low- to moderate-amplitude, moderate-frequency drawing continuous sheeted to disrupted reflectors is unconformably overlying Unit V and locally onlaps onto the basement. The thickness of Unit IV remains rather thin in the northern and eastern Alboran basin. It cannot be properly identified in the southern Balearic basin, east of the Maimonides volcanic ridge (Fig. 15). Unit III, dated from late Serravallian to late Tortonian, is represented by sandstones interbedded with volcano-clastic levels that correlate in EAB with the volcanic vY1 unit. Unit III contains internal reflections characterized by low- to moderate-amplitude, moderate-frequency continuous sheeted reflectors. Its thickness remains relatively constant from the NAB to the EAB and is identified beneath the Messinian Unit II in the southern Balearic basin. Unit II corresponds to the Messinian evaporite, carbonate, volcanic, and volcaniclastic deposits interbedded with fine-grained sediments and is equivalent to unit III of Gómez de la Peña et al. (2020b) in EAB. Seismic facies of Unit II are marked in the Alboran domain by lower amplitudes and lower-frequency reflectors. In ESCI-Alb2b line, Unit II increases drastically east of the Maimonides Ridge, which delimits the western boundary of the salt deposits in the western Mediterranean basin during the Messinian Salinity Crisis (Haq et al., 2020). Unit II is topped by Unit I, which is made of Pliocene to Quaternary clays and sandstones and is correlated with units II and I in EAB (Gómez de la Peña et al., 2020b). Unit I is marked by thinly bedded, mostly parallel, high-frequency and low-amplitude reflectors (Fig. 15). Its thickness fluctuates in response to sedimentary processes (Juan et al., 2016).

Along line MSB08 (Fig. 14) the Langhian–Serravallian (Unit V) is a maximum of 1600 m thick (using a P-wave velocity of 3.2 km s-1 calculated within the Andalucía-A1 well). In EAB, south of the Carboneras fault zone, the total thickness of Unit V is only ∼ 300 m on MSB07 (Fig. 13) and is absent in ESCI-Alb2b (Fig. 15). The Serravallian–Tortonian (units IV–III) interval shows only very limited sediment accumulation (∼ 300 m) except near the NW–SE-oriented normal faults where growth geometries are visible. These normal faults are sealed by the Tortonian–Messinian deposits, indicating a syn-sedimentary faulting during the middle Miocene (Fig. 13). With respect to onshore observations, this sedimentary infill is more continuous and is also much thinner compared to TB and HOB, where they are represented by thick conglomerates and marls or turbidites (> 1 km) (Fig. 7) and are eroded or not deposited along the axes of the metamorphic domes. The Messinian deposits (Unit II) are ∼ 150–350 m thick north of CF (MSB07-08; Figs. 13, 14) and increase to about 1200 m eastward in the eastern EAB (ESCI-Alb2b; Fig. 15) and in the Algero-Balearic basin (Gómez de la Peña et al., 2020b). The top Messinian reflector is topped by thick horizontal sedimentary strata, with a maximum thickness of 1.2 s TWTT (∼ 2.4 km assuming a velocity of 2 km s-1) on line MSB07, suggesting an important channel system during the Pliocene.

The Pliocene to Quaternary series are poorly deformed except in the vicinity of CF and near the Alboran Ridge where this is associated with an S-dipping reverse fault (Fig. 13). This late and still-active compressional tectonic activity is revealed by the overthrusting of the SAB over the south margin of the EAB (e.g. Martínez-García et al., 2011).

Based on subsurface constraints and field data, in Fig. 17 we present a crustal-scale section across the rifted margin, from the Sierra de las Estancias and Huércal-Overa basin (HOB) to the Alboran ridge, that represents the inverted southern margin of the EAB. The proximal margin, where the crust is 30–35 km thick, is defined to the north by the transition between the southern Iberia margin and the metamorphic domain of the Alboran basement exposed in the Sierra de las Estancias. This continental domain preserves part of the crustal thickness acquired during former Betic orogenic phase that has been little involved in crustal thinning. The onset of crustal thinning to the south coincides with the position of the lithospheric tear fault documented by seismology (Fig. 4; Mancilla et al., 2015a) and is recorded by the formation of asymmetric basins of the HOB and TB, shaping the upper neck domain. Orthogonal and oblique extension in this domain is accommodated by normal and strike-slip faulting during the Tortonian. From the Sierra de los Filabres to the south, the thickness of the continental crust reduces to 25 km in the Tabernas basin along the Alpujarras strike-slip fault zone and below the Sierra Alhamilla (Fig. 17). The Nijar basin depicts the transition towards offshore distal domains where the continental crust reaches a thickness of 20 km. The Tortonian and Messinian marine sediments are also thicker. It is worth noting that a number of volcanic bodies offshore (e.g. Chella Bank on MSB08) accompany crustal thinning of the continental crust. The Carboneras Fault (CF) brings crusts with different thicknesses and compositions into contact. South of the CF, the crustal thickness of the EAB is 18 km, and seismic velocities, especially the occurrence of a high-Vp lower crust, have been considered to indicate that the EAB is floored by a magmatic arc crust (Gómez de la Peña et al., 2018, 2020) formed in a supra-subduction context above the subducting Alboran slab (Booth-Rea et al., 2018). The crustal thickness of the EAB is compatible with crustal thinning of the continental margin, and the occurrence of NW–SE-trending faults also recognized onshore despite being slightly older (Serravallian–Tortonian) suggests that the EAB formed under the same back-arc extension setting relative to westward slab retreat (as did the whole Alboran margin). Thus, the magmatic arc crust of the EAB could represent voluminous magmatic intrusions (e.g. Al Mansour dacite or Alboran Ridge rhyolite dated to ca. 9 Ma; Duggen et al., 2004; Tendero-Salmerón et al., 2022; Fig. 17) formed on the distal rifted margin of the Alboran Ridge. The investigation of the causes of calc-alkaline magmatism is beyond the scope of this study, but we suspect it reflects post-subduction arc magmatism induced by remelting during extension and delamination of a metasomatized wedge of mantle lithosphere formed during a previous subduction event (e.g. Richards, 2009). The fact that calc-alkaline magmatism around 10 Ma that is 10 to 5 Myr after the onset of upper plate extension in the Betic–Alboran region supports this view. Note that in contrast to Gómez de la Peña et al. (2020) and Booth-Rea et al. (2018), we implicitly assume the magmatic arc crust of EAB is not a newly formed crust but rather represents a thinned continental crust later intruded by calc-alkaline magmas. Different crustal domains are expected across a rifted margin that has involved a variable amount and different types of mantle-derived magmatism, especially if delamination or subduction occurred during extension. The observation of contrasting types of crustal domains now juxtaposed in the N–S direction is also related to the fact that extension is oriented perpendicular to the section.

Crustal shortening in Fig. 17 is distributed across the north-vergent reverse faults below the Alboran Ridge on the northern limb of Sierra de Alhamilla and the CF strike-slip fault zone.