Geomorphic signature of segmented relief rejuvenation in the Sierra Morena, Betic forebulge, Spain
The foreland relief of alpine orogenic belts is often rejuvenated due to the intraplate propagation of orogenic deformation. Thus, in these long-lived areas, the localisation of relief rejuvenation may be largely controlled by the reactivation of previous mechanical discontinuities. In this regard, we explored the relationship between the relief rejuvenation pattern and the distribution, geometry, and kinematics of faults in a wide segment of the Betic foreland (Sierra Morena, southern Spain). Specifically, we focused on the forebulge, a WSW–ENE flexural relief that formed, paired to the Betic foreland basin, in response to orogenic load. For this purpose, we applied both qualitative and quantitative geomorphological tools, including geomorphic indices and knickpoint pattern modelling in χ space. We found that the pattern of relief rejuvenation responds to large-scale flexural uplift coupled with the tectonic activity of two groups of faults that often show evidence of reactivation, namely overall WSW–ENE faults contributing to both regional NNW–SSE relief segmentation and vertical extrusion of the forebulge, and NW–SE reverse faults associated with an outstanding WSW–ENE topographic segmentation in the west of the study area. In addition, our knickpoint modelling suggests that the faults related to the southernmost Sierra Morena mountain front have been particularly active in recent times, although their activity span and the relative uplift that they accommodate differ along the Sierra Morena/foreland basin limit. The knickpoint pattern also suggests a significant reorganisation of the analysed drainage basins. The strain partitioning accommodated by the structures involved in relief rejuvenation suggests the intraplate propagation of the transpressional deformation reported from the Betic external fold and thrust belt.
Relief rejuvenation of geologically ancient areas often occurs in response to intraplate deformation. In these long-lived areas, the reactivation of pre-existing structures is a common mechanism for strain accommodation, which is often favoured over the generation of new structures (e.g. Butler et al., 1997). Thus, previous discontinuities can be expected to localise the relief rejuvenation associated with recent or active tectonics, which can therefore be analysed to delve into the kinematics of recent deformation.
The relief of the Variscan basement outcropping in the western and central Iberian Peninsula is characterised by roughly W–E or WSW–ENE topographic highs (1000 to 2500 m a.s.l.) separated by Cenozoic sedimentary basins (Fig. 1a). On the basis of both numerical and analogue models, these topographic domains have mainly been interpreted as the expression of lithospheric folding (Cloethingh et al., 2002; Fernández-Lozano et al., 2012) due to the superposition of successive intraplate deformation phases from the Late Cretaceous–Early Cenozoic onwards. They have been mainly associated with plate boundary activity both to the north (Pyrenean–Cantabrian orogen; e.g. Roest and Srivastava, 1991; Teixell et al., 2018) and to the south (Gibraltar Arc; e.g. Spakman and Wortel, 2004; Balanyá et al., 2012) of Iberia (Fig. 1a). In the upper crust, such intraplate deformation is often accommodated by the reactivation of pre-existing faults, which largely control the spatial distribution and orientation of the topographic features (De Vicente et al., 2007; Martín González, 2009; Brum da Silveira et al., 2009; Vázquez-Vílchez et al., 2015).
The southernmost topographic high (900–1300 m a.s.l.) within Variscan Iberia is Sierra Morena (Fig. 1a and b). It is a WSE–ENE relief, approximately 600 km long and 80 km wide, and WSW-ENE relief, the southern limit of which coincides with a regional linear escarpment separating the foreland (i.e. the Variscan Iberian Massif) from the Cenozoic Guadalquivir foreland basin of the Betic Chain (northern branch of the Gibraltar Arc). Sierra Morena as a whole is interpreted as a forebulge, a positive relief that develops, paired with foreland basin subsidence, due to lithospheric flexure in front of major fold-and-thrust belts (e.g. Flemings and Jordan, 1990; DeCelles, 2012, and references therein). In this tectonic context, the Sierra Morena forebulge uplift is linked to the lithospheric flexure of the Iberian Massif under the Betics orogenic wedge load, enhanced by the buckling of the Iberian lithosphere (Cloething et al., 2002; García-Castellanos et al., 2002). Concerning this folding, a NW–SE-oriented compression, connected to the convergence between Africa and Eurasia, is invoked for the neotectonic intraplate deformation of Iberia (Herraiz et al., 2000; Cloething et al., 2002).
This interpretation of the overall Sierra Morena relief as a flexural forebulge folded by NW–SE-oriented buckling is mainly based on the numerical modelling of the lithosphere rheological behaviour (Cloething et al., 2002; García-Castellanos et al., 2002). Nevertheless, little work has been done to address the geomorphological imprint of this tectonic model in Sierra Morena.
In this regard, previous studies propose that the tectonic setting for the current deformation of the western Betic fold-and-thrust belt (FTB) includes the westward migration of the Gibraltar Arc hinterland (Balanyá et al., 2012; Gutscher et al., 2002). This would imply that the tectonic mechanism responsible for the Miocene accretion of the Betics (e.g. Faccenna et al., 2004; Balanyá et al., 2007) is still active. Additionally, analytical and analogue models (Díaz-Azpiroz et al., 2014; Barcos et al., 2015, 2016) provide a N99∘ E–N109∘ E trending horizontal velocity vector to explain the Neogene to recent dextral transpressional kinematics observed in segments of the western Betic FTB (see also García et al., 2016; Jiménez-Bonilla et al., 2015). This velocity vector orientation fits well with such a westward motion of the hinterland relative to the FTB.
Irrespective of the current tectonic setting, Neogene, or even younger, activity has been reported in specific areas of Sierra Morena. Thus, in the Guadiamar drainage basin (westernmost Sierra Morena; GB in Fig. 1c), river migration due to Holocene regional tilting has been described (Salvany, 2004). Additionally, seismicity consistent with reactivation of pre-existing fractures has been pointed out in the Sierra Albarrana area (SA in Fig. 1c; Herraiz et al., 1996), and the upper Miocene infill of the Guadalquivir foreland basin appears locally intersected by faults (Expósito et al., 2016; Matas et al., 2010a).
In this study, we assume that this recent tectonic activity, linked to intraplate tectonics, must have rejuvenated the Sierra Morena relief. Therefore, its geomorphological features must be an expression, among other factors, of its current tectonic setting. Furthermore, we expect that the Sierra Morena relief rejuvenation pattern is significantly conditioned by the reactivation of those previous structures that are favourably oriented.
In this regard, here we analyse the relief rejuvenation of an approximately 130 km long segment of Sierra Morena (Fig. 1b), which is potentially related to the recent reactivation of pre-existing structures in the Betic foreland. To this end, we first analyse the space distribution of key geomorphic features that would characterise relief rejuvenation, i.e. preserved relicts of Miocene landscape surfaces, patches of shallow-water marine Miocene deposits, incised meanders, active knickpoints, perched terraces, stream gaps, and piracy. Second, we localise the discrete tectonic structures that accommodate differential uplift and relief segmentation within the forebulge. We therefore carried out qualitative landform interpretations and quantitative analyses focusing on tributary drainage networks located on the Guadalquivir river right bank, i.e. those streams draining the Betic forebulge southward. The kinematics of these reactivated structures will be used in this study to explore the recent, even current, tectonic scenario compatible with the observed reactivation pattern. Finally, we will discuss previous geophysical data (Herraiz et al., 2000; De Vicente et al., 2007) and relief modelling (García-Castellanos et al., 2002), as viewed from the newly obtained geomorphological and structural data.
Our results prove that the characterisation of relief rejuvenation patterns together with the kinematic analysis of the main relief-controlling structures provides information about both the role of reactivated structures in the relief rejuvenation modes and the tectonic setting in which rejuvenation occurs.
In this study, we analyse an approximately 130 km long segment of the western and central Sierra Morena, including its boundary with the Guadalquivir river valley (Fig. 1). This topographic limit coincides with the contact between two geological units, i.e. the Betic foreland to the north, constituted by the Iberian Massif, and the Betic foreland basin to the south.
The Iberian Massif crops out in western and central Iberia, also constituting the buried basement of the main Cenozoic basins (Fig. 1a). This geological domain belongs to the Variscan chain, a late Paleozoic orogenic belt, which extends from Morocco to central Europe. Regarding its distinctive tectonic features, the southernmost Iberian Massif has been divided into three different zones, from SW to NE, namely the south Portuguese Zone (SPZ), the Ossa-Morena zone (OMZ), and the central Iberian zone (CIZ). Most of our study area belongs to the SPZ and the OMZ, with the CIZ only being represented in its NE limit (Fig. 1b).
In our study area, the SPZ is composed of pre-orogenic Devonian to Carboniferous metadetritics, profusely intruded by igneous rocks, which are locally covered by unconformable post-orogenic Permian sequences (e.g. Oliveira, 1990; Simancas, 1983). In its northern limit, a narrow band of slates with interbedded tuffites and quartzites crops out (Matas et al., 2010b). The OMZ and the CIZ are mainly formed by Neoproterozoic to Carboniferous metadetritic rocks, although lower Cambrian carbonate formations are well represented. Volcanics are frequently interbedded in the Neoproterozoic rocks of both zones and in the lower Cambrian to Ordovician sequences of the OMZ. Plutonic rocks mainly crop out related to the SPZ/OMZ and OMZ/CIZ boundaries (Matas et al., 2010a, b).
The current regional limit between the OMZ and the SPZ is located along the transpressive, from the top to the SW, southern Iberian shear zone (Fig. 1b). It is interpreted as part of a complex, long-lived Variscan suture, including amphibolites of oceanic affinity and high-pressure/low-temperature rocks (e.g. Crespo-Blanc and Orozco, 1988; Díaz-Azpiroz and Fernández, 2005; Fonseca and Ribeiro, 1993; Simancas et al., 2003; Pérez-Cáceres et al., 2015, and references therein). In our study area, this boundary is hidden to the SE under the infill of the Permian Viar basin (Figs. 1b and 2a), a NW–SE elongated outcrop, interpreted as a late Variscan intramontane basin with an infill made up of lower Permian detrital and volcanic rocks (Simancas, 1983; García-Navarro and Sierra, 1998). According to previous interpretations, the basin would have been inverted from the end of the early Permian to the Middle Triassic (García-Navarro and Fernández, 2004). This inversion would have produced both an open N150∘ E-oriented syncline and the NW–SE Viar reverse fault system (VFS) along its NE limit. This Permian sedimentary basin coincides with the current River Viar drainage basin (Fig. 1b) downstream of the VFS.
In our study area, the Iberian Massif records a complex Variscan deformation characterised by mainly Devonian to lower Carboniferous, NW–SE trending, folds and thrusts (e.g. Expósito et al., 2002; Mantero et al., 2011; Simancas et al., 2003). It should be noted that pervasive fractures of diverse orientation and kinematics have been reported to cut the main Variscan structures in our study area. Many of them have been attributed to the late stages of the Variscan deformation (e.g. García-Navarro and Fernández, 2004), although fractures with Cenozoic activity have been often reported close to the Iberian Massif/Guadalquivir foreland basin limit (e.g. Matas et al., 2010a; Expósito et al., 2016; Vázquez-Vílchez et al., 2015).
During the Mesozoic tectonic evolution of southern Iberia, the Iberian Massif relief was attenuated towards the SE by the formation of the rifted south Iberian paleomargin, separated from the continental Alboran Domain margin by the Tethys Ocean (Dercourt et al., 1986; Faccenna et al., 2004). The westward migration of the Alboran Domain led to the closure of this alpine oceanic basin in the early Miocene, giving rise to the formation of the Betic Chain on the southern Iberian paleomargin (Balanyá and García-Dueñas, 1987). In the middle Miocene, the Betic orogenic load provoked the lithospheric flexure of the Betic foreland (Van der Beek and Cloetingh, 1992), thus creating the Betic foreland basin (i.e. the Guadalquivir foreland basin) coupled with the forebulge just to the north of the Betic mountain front (García-Castellanos et al., 2002). The Guadalquivir foreland basin remained as a marine basin connected to the Atlantic Ocean from the middle Miocene to the beginning of the Pliocene when the asynchronous westward uplift of the basin led to the coast migration to the SW (e.g. Fernández et al., 1998; González-Delgado et al., 2004; Sierro et al., 1996). During the Quaternary, the Guadalquivir river drainage system evolved, and the upper Miocene shallowing-upward marine sediments were partially covered by alluvial deposits.
In our study area, the oldest infill of the Guadalquivir foreland basin corresponds to Tortonian calcirudites and calcarenites, which unconformably overlie the pre-Mesozoic rocks of the basement. On top of them, Messinian basinal deposits are represented by marly clays. Quaternary deposits consist of alluvial conglomerates, sands, silts, and clays related to the Guadalquivir river floodplain and to an extensive strath terrace system (Moral et al., 2013).
As previously mentioned, the southern boundary of the Iberian Massif basin also separates two distinctive relief domains, i.e. Sierra Morena to the north and the Guadalquivir river alluvial plain to the south, which is set on the most low-lying areas of the Guadalquivir foreland basin.
The main summits of Sierra Morena are 900 to 1300 m a.s.l. (above sea level) and 900–1000 m a.s.l. in the study zone. Traverse topographic profiles across Sierra Morena present a remarkable asymmetry. The relief of the main mountain ridges related to the southern Iberian sub-plateau and the Guadalquivir valley is about 300–400 and 800–900 m a.s.l., respectively. Furthermore, the northern boundary of Sierra Morena is a gently dipping transitional piedmont, whereas the southern boundary coincides with a well-defined escarpment of low sinuosity.
The NW–SE orientation of the main streams draining the southern slope of Sierra Morena is determined in their upper reaches by the Variscan orogenic grain (Fig. 1b and c). Nevertheless, the Variscan residual relief gradually disappears toward the limit with the Guadalquivir river basin and is substituted by an erosional relict surface of plausible middle–late Miocene age (Yanes et al., 2019).
At the foot of Sierra Morena, the Guadalquivir river valley is a WSW–ENE-oriented depression limited to the east and south by the Betic mountain front and to the west by the Atlantic Ocean. In our study area, it is characterised by an overall low-lying relief, with altitudes ranging between 30 and 200 m a.s.l. in the Neogene sediments and between 10 and 100 m a.s.l. in the Quaternary alluvium. Nevertheless, its easternmost sector exhibits a moderately rugged topography, with elevations that reach up to 800 m a.s.l. Furthermore, the Guadalquivir river is in a markedly asymmetric position, located at the northern edge of both its valley floor and alluvial deposits. Terraces that developed on the wider left-hand slope of the Guadalquivir river valley are gently tilted northwards (Moral et al., 2013).
As stated above, the characterisation of the Sierra Morena relief rejuvenation pattern and the identification of the structures localising such rejuvenation are crucial for our study objective. First, we have searched for signs of relief rejuvenation by applying both geomorphic qualitative methods and geomorphic indices. The purpose of this was to detect the key relief features of relief rejuvenation and the potential involved structures (mainly faults). We then proceeded to use field-based structural analysis methods to determine the kinematic regime of these faults by means of different kinematic indicators such as slickenlines or brittle S-C fabrics.
Our analysis focused on six main drainage basins showing signs of relief rejuvenation. They are located on the right slope of the Guadalquivir river valley, i.e. those draining southern Sierra Morena (Fig. 1b). Additionally, some minor sub-basins have also been included (see also Fig. 2a). For this, we used the 12 m resolution TanDEM-X digital elevation model (DEM; Wessel, 2016).
In terms of the qualitative approach, we focused our attention on those drainage network features indicative of relief rejuvenation (stream piracy, wind or water gaps, incised meanders, etc.) and on the geometry and distribution of a Miocene erosional relict surface that often occupies interfluves. Our qualitative analyses are based on the landscape morphometry, which has been characterised by means of local relief maps (difference between maximum and minimum elevation by using neighbourhood statistics; 15×15 pixels) and slope maps. We also applied several geomorphic indices, often used in low-rate tectonic regions (e.g. Silva et al., 2003; Perez-Peña et al., 2009), to better determine the recent tectonic activity associated with the main mountain fronts. After that, we analysed the kinematics of those structures with a position and geometry that are compatible with the observed modes of relief rejuvenation.
Finally, we tested the relationship between those structures associated with the main rejuvenated mountain fronts, the distribution of knickpoints on river profiles in χ space (Perron and Royden, 2013; Schwanghart et al., 2021), and the drainage divide network migration (Scherler and Schwanghart, 2020; Schwanghart and Scherler, 2020). This analysis enables us to delve further into the relationship between the analysed faults and the current drainage dynamics. It also sheds light on the relative relief rejuvenation among the drainage basins linked to the fault activity in Sierra Morena.
3.1 Geomorphic indices
We calculated several quantitative geomorphic indices on selected areas of interest, which are very sensitive to changes in the river equilibrium profile.
Mountain front sinuosity, Smf (Bull and McFadden, 1977; Bull, 1978), was defined as follows:
where Lmf is the length of the mountain foot, and Ls is the length of the straight line that links the mountain front tips. Values of 1 indicate a straight front geometry potentially related to recent tectonic activity of faults. Nevertheless, Smf values also depend on factors such as the lithology and fault dips (Keller and Pinter, 2002; Jiménez-Bonilla et al., 2015). To avoid bias in our results, we applied Smf to mountain fronts related to faults dipping between 60 and 80∘ that bring similar lithologies into contact. Mountain fronts were divided in segments between 2 and 10 km long. The slope break line determining the position of mountain fronts was established at slope values of 8∘.
Valley floor-to-height ratio, Vf (Bull and McFadden, 1977), was calculated for streams that run perpendicular to mountain fronts. Vf is defined as follows:
where Vfw is the width of the valley floor, Eld and Erd are the elevations of the left and right valley divides, respectively, and Esc is the elevation of the valley floor.
Two types of valleys are traditionally distinguished according to Vf values (e.g. Keller and Pinter, 2002; Silva et al., 2003; Giaconia et al., 2012; Jiménez-Bonilla et al., 2015). V-shaped valleys (Vf<1) are associated with active down-cutting streams, while flat-bottomed valleys (Vf >1) testify to large lateral erosion and/or sedimentation related to relatively tectonic quiescence. This index has been combined with Smf in previous work as a proxy to test recent tectonic activity (e.g. Silva et al., 2003).
The drainage basin hypsometric curve shows the normalised basin area () above a normalised altitude (; Strahler, 1952). The shape of the hypsometric curve has been related to the degree of the dissection of the basin. Upward convex hypsometric curves are associated with young and weakly eroded basins, while concave curves indicate highly eroded basins. S-shaped curves are frequently associated with moderately eroded basins (e.g. Keller and Pinter, 2002); however, they can also feature residual reliefs that have recently been uplifted and reactivated (e.g. Azañón et al., 2012), i.e. relief rejuvenation. This is the reason why special attention was paid to S-shaped curves. The area below the hypsometric curve, which ranges between 0 and 1, is the hypsometric integral (HI; e.g. Keller and Pinter, 2002). Values close to 1 indicate weakly eroded regions.
We have plotted the hypsometric curve and calculated HI values for several right tributaries of the Guadalquivir river.
3.2 χ space analysis of river profiles
3.2.1 DEM correction and knickpoints extraction
Pre-processing was performed in order to correct longitudinal profiles prone to data artefacts. Thus, the frequent presence of artificial dams in Sierra Morena constitutes a source of error that affects the quality of the knickpoint analysis results. To tackle this issue, we first mapped all the artificial dams and the tributary inlets into artificial lakes. The detection of artificial dams was performed through remote sensing data, such as Google Earth satellite optical images (2018 Landsat Imagery).
The TopoToolbox “mincosthydrocon” function (Schwanghart and Scherler, 2014) was used for the correction with the min–max method. Afterwards, we analysed selected stream networks upstream of fault segments, mostly located at the Sierra Morena southern mountain front, exhibiting qualitative signals of relief rejuvenation.
On each basin, we extracted knickpoints using the TopoToolbox “knickpointfinder” function (Schwanghart and Scherler, 2014, 2017). The estimate of the uncertainty was performed using the constrained regularised smoothing or CRS technique (Schwanghart and Scherler, 2017). The tolerance value obtained by the CRS application is 38 m.
3.2.2 χ transformation of longitudinal river profiles
For the river profile analysis, we applied the integral approach introduced by Perron and Royden (2013) of the stream power incision model (SPIM; Lague, 2014). According to the SPIM, the evolution of the river profile is described as the change through time t in elevation z of a channel point located at an x upstream horizontal distance, which can be calculated using the following expression:
where U is the uplift, A is the drainage area, m andn are positive an empirical constants, and K is the erodibility.
If both processes are perfectly balanced, then a state of a dynamic equilibrium or steady state () is assumed. In this case, the Eq. (3) can be rearranged as follows:
where U and K do not vary in time and in space, and the drainage configurations remain unchanged. Equation (4) predicts a power law relationship between the slope and drainage area A (Hack, 1957).
Perron and Royden (2013) proposed a transformation of the horizontal spatial coordinates which linearises the power law relation by the integration of , with respect to x, from a base level xb to an arbitrary upstream point x in the channel.
where A0 is an arbitrary scaling area. Performing the integration, Eq. (5) becomes the following:
Even if a river is not in a topographic steady state, the advantage of using the χ plot of its longitudinal profile is that transient signals with a common origin (e.g. fault-related knickpoints) propagating upstream through different channels, along either the main stem or tributaries, plot in the same location in the transformed coordinate χ (Perron and Royden, 2013; Schwanghart and Scherler, 2020). Additionally, in steady-state conditions, the main stem and tributaries become aligned once the best value has been determined. Thus, transient signals are easier to identify when the transformed profiles deviate from such trend. Thus, χ serves as a metric for distances travelled by perturbations upstream in the river network (Fox et al., 2014). For this reason, we consider this to be the base level xb of the intersection between streams and fault traces. Furthermore, to find the best value for each basin, i.e. with the best-fit linear relationship between χ and elevation (Perron and Royden, 2013), we used the TopoToolbox “mnoptimvar” and “robustcov” functions (Schwanghart and Scherler, 2014). This function finds the value that minimises the χ disorder, which is intended as the variability in elevation values for similar values of χ (Hergarten et al., 2016).
Finally, according to Eq. (6), the slope of the χ profiles is dependent on the uplift rate and the erodibility because it increases as the uplift rate (U) increases and decreases as the erodibility (K) increases. In general, the χ slope is a proxy for the actual erosion rate, which can be transferred to uplift rates only for equilibrium conditions. In this regard, we assume that there are no strong lithological contrasts in the study area, justifying that the lithological control on fluvial erosion is quite homogeneous (K constant). Then, the slope of the χ plots can be interpreted to be a proxy for the tectonic activity. In this sense, the uplift U can be considered constant for each analysed basin, since each one depends on a different fault, and the upstream area can be assumed as an uplifted block.
3.2.3 Knickpoint pattern modelling
In order to cluster the different knickpoint sequences associated with fault activity, we implemented a parametric density distribution technique using the TopoToolbox “rhohat” function (Schwanghart et al., 2021), which also calculates confidence intervals using bootstrapping. In this regard, we estimated the dependence (ρ) of a spatial process (knickpoints) on a spatial covariate (χ-transformed distance from the outlet), implementing the calculus of the parametric density distribution weighted by the knickpoint height. The knickpoint height is the elevation difference between the fitted profile and a knickpoint. The number of bootstrap samples was set to 10 000, while the bandwidth of the Gaussian kernel was 250 m. In addition, 95 % bootstrapped confidence intervals were set.
In order to isolate the bias due to the artificial dam's artefacts, we compared ρ values obtained with the entire dataset with those obtained when removing knickpoints associated with artificial dams.
3.3 Drainage divide network analysis
The divide network, and its relation to topography, has been analysed to investigate possible inconsistencies between expected and observed knickpoint patterns. For that purpose, we followed the method described in Scherler and Schwanghart (2020). In detail, we extracted drainage divides based on the drainage basin boundaries that we obtained for drainage areas at tributary junctions and drainage outlets. We then organised the collection of divide segments into a drainage divide network and ordered it with ordering scheme of “Topo” (according to the name of the algorithm), for which divide orders increase by 1 at each junction. Regarding topographic metrics, Scherler and Schwanghart (2020) focused on the hillslope relief (HR), defined as the elevation difference between a point on the divide and the point on the river that it flows to. To quantify the morphologic asymmetry of a divide, the across-divide difference in hillslope relief (ΔHR) is normalised by the across-divide sum in hillslope relief (∑HR). The divide asymmetry index (DAI) was subsequently computed as follows:
The DAI ranges between 0 for entirely symmetric divides and 1 for the most asymmetric divides.
4.1 Geomorphological features
The relief of the southern half of Sierra Morena is mainly characterised by planar summits alternating with incised valleys (Fig. 1c). Summits are regionally oriented in a sub-horizontal attitude or dip slightly towards the Guadalquivir valley (e.g. Figs. 2b and 3a), although some exceptions have been found locally. Examples of this anomalous dip have been observed north of Córdoba (Fig. 4), where the upper edge of the SW–NE Sierra Morena escarpment coincides with the Guadiato eastern divide. This northwestward tilting occurs east of a river elbow testifying stream piracy along the Guadiato stream. As a result, the Guadiato stream bends to the NW, thus leaving a roughly N–S-oriented wind gap south of the piracy (see also Fig. 11b and d).
These summits often represent remnants of an erosional peneplain which has previously been dated to the Paleogene (Rodríguez Vidal and Díaz del Olmo, 1994). Nevertheless, their location adjacent to the Guadalquivir foreland basin suggests that the relict surface shaping must have been controlled by the local base level of this uplifted marine basin, which was active during the middle–upper Miocene (Yanes et al., 2019). Locally, summits are occupied by patches of Neogene shallow marine sediments belonging to the Guadalquivir foreland basin. They unconformably overlie the pre-Mesozoic basement and are uplifted several tens, or even hundreds, of metres above their equivalent in the Guadalquivir river valley (e.g. Figs. 1b and 4a, b). Irrespective of their nature, flat summits often describe a roughly N–S stepped relief segmentation, i.e. parallel to the Sierra Morena southern boundary.
Additionally, there is significant WSW–ENE segmentation of the Miocene relict surface across the Permian Viar basin, which partly coincides with the River Viar lower drainage basin (Fig. 2a). This NW–SE depression is open to the Guadalquivir river valley. The average elevation of its low-lying relief is similar to that of the hills shaped on the Miocene and Plio-Quaternary rocks of the northern Guadalquivir valley. The Permian Viar basin is flanked by NW–SE-oriented ranges, markedly incised by tributaries on both the right and left banks of the River Viar. The resulting summits have smooth slopes that rarely exceed 5∘ towards the SSE (Fig. 2b). In contrast, their boundaries with the Permian Viar basin are abrupt, with averages slopes of 45 % on its eastern boundary, coinciding with the VFS trace, and 20 % on its western boundary. When compared on both sides of the VFS trace, the erosional relict surface located on the OMZ summits (i.e. the hanging wall) is at a higher topographic level (up to 100 m higher) than on the SPZ summits (i.e. VFS footwall; Fig. 2b).
Drainage networks mainly follow a dendritic pattern paired with local parallel networks. The main streams trend NW–SE in their upper reaches – following the Variscan orogenic grain – and bend N–S close to the boundary with the Guadalquivir valley (Fig. 1b). This is conditioned by the southward increasing topographic gradient between the Iberian Massif and the Guadalquivir basin. Secondary stream orientations, however, are often controlled by fractures, particularly in the SPZ, where lower-order streams of the River Viar follow the trend of SW–NE to W–E fractures (Fig. 2a).
Streams often display features associated with relief rejuvenation, such as perched terraces or stream elbows, due to both fault-related stream deflections (e.g. Fig. 3b) and river capture (e.g. Figs. 3d and 4a). Furthermore, incised meanders are significantly abundant in Sierra Morena (e.g. Fig. 3c and d). These meanders run along valleys that can be hundreds of metres below summits and develop steep slopes (locally up to 70 %–80 %). Long profiles of both main and secondary streams often show typical non-equilibrium, upward-convex geometry (Fig. 9) and display knickpoints that are not related to lithological contrast. A long profile analysis will be carried out below in Sect. 6.
4.2 Geomorphic indices
A quantitative analysis (Fig. 5) was performed on six drainage basins belonging to the main right tributary streams of the Guadalquivir river (S1 to S6 in Fig. 1b). From west to east, these basins belong to the following rivers: Rivera de Huelva–Cala (S1), Viar (S2), Guadalbarcar (S3), Retortillo (S4), Bembézar (S5), and Guadiato (S6). Most of these rivers are particularly incised upstream of the Sierra Morena southern mountain front. An exception is the River Viar (S2), for which the incision occurs upstream of the VFS. Additionally, some second-order tributaries within S2 have also been analysed by means of geomorphic indices.
Overall, those mountain fronts related to the southern Sierra Morena escarpment yield low Smf values, thus corresponding to straight mountain fronts (Table 1). In detail, those values obtained for segments of the WSW–ENE Sierra Morena escarpment vary from 1.15 to 1.3. In the same way, Smf related to the Permian Viar basin's eastern boundary, i.e. coinciding with the VFS, are between 1.2 and 1.4. Values obtained for the western boundary are slightly higher and are between 1.2 and 2.0.
As describe in Sect. 4, the Sierra Morena relief mostly consists of roughly flat, sub-horizontal, or gently south-southeastward dipping summits separated by incised valleys. These summits often exhibit either remnants of an upper Miocene relict peneplain or upper Miocene rocks deposited in the Guadalquivir foreland basin. Therefore, these relief elements must have been relatively uplifted from their initial position, i.e. at the Guadalquivir basin level, after the late Miocene. Given that we have discarded vertical faults and avoided lithological contrasts, straight mountain fronts (close to 1) indicate young, non-eroded escarpments. This indicates that the southern Sierra Morena relief has been rejuvenated by Quaternary activity of the escarpment-related faults.
Vf values are less than 1 (Table 1 and Fig. 5a), therefore associated with V-shaped valleys, when measured just upstream from both the Sierra Morena escarpment and the VFS. Conversely, these values are systematically greater not only downstream from the mountain fronts but also in the upper reaches of the analysed streams. In theory, the VF value along a graded long profile tends to increase gradually towards the river mouth. This does not happen in the analysed rivers, where values drop abruptly upstream from the fault-related mountain fronts. Additionally, values are lower in the escarpment sector (quite close to the river mouth) than in the higher reaches of the same river, thus suggesting that the main river incision responds to the slope disequilibrium located in the fault-related escarpment.
Hypsometric curves for S1 to S6 main streams display dominant upward-convex geometries (Fig. 6b) with HI values > 0.5 (Table 1 and Fig. 5b). S5 and S6 curves are slightly S-shaped, with relatively high values in the middle course, thus also showing the lowest HI values. This may indicate that relief rejuvenation is localised in its lower course.
These results suggest, in principle, the relief rejuvenation of their watersheds. However, previous works have pointed out that the basin's hypsometry can be conditioned, among other factors, by the catchment size (e.g. Hurtrez et al., 1999, and references therein). In this regard, the hypsometry of small catchments may be dominated by hillslope processes, leading to upward-convex hypsometric curves. Nevertheless, our selected catchments are large-scale catchments (Table 1), where S1, S2, S5, and S6 are larger than 1000 km2 (up to 1875 km2 in the case of S1), and S3 and S4 are of several hundreds of squared kilometres. Thus, we can assume that the analysed catchments' hypsometry is dominated by river processes, and therefore, the obtained convex upward curves and high HI values can be taken as a proxy for recent tectonics.
Regarding the sub-catchments of S2 (Figs. 1b, 2a, and 5c), they are small-scale basins (between 18 and 71 km2). S2.4, S2.5, and S2.6 are located on the hanging wall of the VFS, being therefore in the same tectonic situation as the S2 mainstream (i.e. the River Viar; Fig. 5b). Despite being 2 orders of magnitude smaller, the geometry of both their hypsometric curves and their HI values is similar to the those of S2 mainstream. This seems to indicate that the hypsometry of the catchments located on the VFS hanging wall is significantly conditioned by the Quaternary reactivation of such a fault system.
Similar hypsometric curves geometries and HI values have been obtained for the right slope tributaries of the River Viar (S2.1, S2.2, and S2.3; Figs. 1b and 5c), indicating that the SW boundary of the Permian Viar basin has also undergone relief rejuvenation.
As described in previous sections, the topographic distribution of Sierra Morena is regionally defined by a NNW–SSE segmentation that is primarily localised in the Sierra Morena southern slope break, but that also extends northwards, often conditioning the orientation of the secondary stream networks (e.g. Fig. 2a). Thus, this segmentation is defined not only by the topographic step at the southern limit of Sierra Morena but also by the tilting and displacement, to the north, of both the Miocene erosional paleo-surface and Miocene marine deposits (e.g. Figs. 2b and 4b, d).
We have found that this NNW–SSE segmentation is spatially related to faults that trend from SW–NE to WNW–ESE, with the former being the best represented (Fig. 6). Most of them exhibit steep surfaces that dip with either a N or S component. Their slickensides indicate slip senses that vary from the dominant normal dip slip to the dominant right-lateral slip, with the oblique, right-lateral normal faults being well represented. Although the normal slip component is dominant, a reverse component also occurs.
Some of these faults involving Paleozoic rocks seem to have been formed by the reactivation of previous structures. For example, in igneous rock outcrops of both the SPZ and the Permian Viar basin, these faults are evenly distributed with a spacing of metric order, thus pointing to the reactivation of previous joints. In the same way, slickensides indicating normal to dextral faults have been observed along the WSW–ENE Embalse del Cala fault (Figs. 2a and 3c), which is a Variscan, left-lateral structure located west of the Permian Viar basin (García-Navarro and Férnandez, 2004).
As mentioned above, this fault system is particularly developed in the Sierra Morena escarpment, defining its southern mountain front. The presence of both relict surface remnants and shallow-water Miocene rocks along the top of the escarpment enables a minimum vertical throw of the Paleozoic basement to be established. This vertical throw seems to have been greater in the east of our study area (up to 480 m north of Córdoba to the south of S6; Fig. 4b–d), gradually decreasing toward the west (≈50 m west of the Permian Viar basin to the south of S1; Fig. 2a). In the eastern sector, the vertical throw is clearly exhibited by the abrupt W–E to SW–NE escarpment located to the NW of Córdoba. At its foot, escarpment-derived colluvium of debris facies can be observed, both pre- and post-dating the Medina Azahara archaeological site (Fig. 4a), which was abandoned and vandalised soon after 1036 (López-Cuervo, 1983). In the northernmost archaeological site, the most recent colluvium (ca. 2 m thick) seals part of the ancient buildings and incorporates scarce fragments of material from Medina Azahara buildings, such as ceramic tiles and wall bricks.
In addition to this regional NNW–SSE relief segmentation, a significant WSW–ENE relief segmentation also occurs across the Permian Viar basin (Fig. 2), i.e. roughly parallel to the overall Sierra Morena escarpment trace. In the NE limit of the Permian Viar basin, this segmentation is markedly localised along the VFS, which consists of mainly NW–SE trending faults. They present moderate to steep northeastward dips, and their slickensides indicate reverse left-lateral slip (Fig. 6d).
In contrast to the NE boundary of the Permian Viar basin, relief rejuvenation in its SW boundary does not seem to be conditioned by NW–SE-oriented faults but is rather significantly distributed in diverse structures. Here, the SPZ rocks are unconformably overlain by gently northeastward Permian rocks (SW limb of the Viar synform), and signs of relief rejuvenation seem to be mostly related to the WSW–ENE fault system. The different relief rejuvenation modes observed to the SW and NE of the Permian Viar basin explain that, although HI yields similar values for both boundaries, Smf values are higher in the SW (i.e. the SPZ/Viar basin boundary). Here, differential uplift does not seem to be accommodated by a discrete structure such as the VFS but rather mainly accommodated by distributed structures of limited extent.
The geomorphological and structural dataset in previous sections suggests that the relief rejuvenation and segmentation observed in our studied area is related to two main fault systems that operated coupled with the regional flexural uplift of the forebulge area. The first one consists mainly of WSW–ENE-oriented faults, which are highly localised along the similarly oriented southern Sierra Morena mountain front. The second one is the NW–SE-oriented VFS, which limited the Permian Viar basin to the NE (Figs. 1b and 2a).
All the analysed basins are crossed in their lower reaches by one of these fault-bounded mountain fronts (Fig. 7), which are either related to the Sierra Morena slope rupture (S1, S3, S4, S5, and S6) or to the VFS (S2). Thus, the drainage network located upstream of faults may have recorded their activity through knickpoint migration.
In this regard, the distribution of the knickpoints upstream of the fault-related main mountain fronts is analysed in this section, and the distribution is compared with that predicted by our knickpoint pattern models (Schwanghart et al., 2021). This analysis will enable the comparison of recent tectonic activity along different sectors of Sierra Morena and enable the deviation between observed and predicted knickpoints to be explored in terms of divide network reorganisation.
To perform χ transformations of longitudinal river profiles, we first calculated the ratio for each basin in Eq. (8) that minimises the variability in elevation values for similar values of χ (Fig. 8). The obtained values indicate that the larger catchments (S1, S2, S5, and S6) are consistent with the widely used reference value , while the smaller ones (S3 and S4) show lower values. Since all considered catchments are similar concerning their fluvial erosion characteristics, a reference value was used for all the catchments in order to compare χ values and thus the locations of knickpoints across catchments.
Figure 9 shows the position on both the mainstream and tributary longitudinal profiles for basins S1 to S6. Horizontal coordinates are displayed for both the regular distance (left side) and χ space (right side). Coordinates (0, 0) correspond to the intersection between the mainstream and the fault-related mountain front. Artificial dams and tributary inlets into reservoirs are also projected along profiles. Finally, covariance estimates (ρ) for knickpoint patterns on a spatial covariate (χ transformed distance from the outlet) are reported with and without artificial dams.
The longitudinal profiles of main streams, except for S4, are partially conditioned by the presence of dams, with this being of particular note in S1, which exhibits five dams distributed over 100 km. Despite these dam-related interruptions, the S3 and S4 longitudinal profiles seem to display a slightly concave-upward shape, whereas those corresponding to S2 and S6 show a conspicuous convex-upward geometry.
The knickpoint distribution along profiles presents certain differences from one drainage basin to another. In S2, S5, and S6, most of the knickpoints are related to the middle and lower values of both x (Fig. 9c, i, and k) and χ (Fig. 8d, j, and l). Conversely, knickpoints are evenly distributed along S1 plots (Fig. 9a and b). Finally, the scarce knickpoints of S3 and S4 are located in middle and high values of the horizontal coordinates (Fig. 9e–h).
The χ space profiles offer a better perspective for discussing the knickpoint pattern dependence. Indeed, the covariance estimate (both with and without artificial dams) highlights how the majority of the higher knickpoints are in the lower part of S1, S2, S5, and S6, whereas in the upper part, several minor knickpoints form secondary peaks in the covariance trend. Knickpoints are particularly clustered in S2, where most of them are distributed in a very narrow strip corresponding to the lower part of the drainage basin, with χ values around 1000–1700 m and elevations around 200 m above the outlet point. Furthermore, S6 knickpoints are clearly grouped in the lower part of the basin, though to a lesser extent than in S2, with χ values between 2000 and 3500 m and elevations between 200 and 400 m above the outlet point.
From the comparison of the covariance computed with and without artificial dams in the dataset, it can be observed that the dependence of the knickpoint pattern is variably affected by the occurrence of artificial dams. In this regard, such a dependence is strong in S1, S3, S5, and S6, as can be inferred by the shifting of the intensity peaks when covariate values obtained with and without dams are compared. However, the dependence of the knickpoint pattern to artificial dams does not seem to be significant in S2, thus only slightly raising the intensity peak of the plot. S4 is not at all biased, since no knickpoints were automatically extracted that coincide with the only artificial dam of this drainage basin. In this regard, the plano-altimetric configuration of some dams cannot exclude the pre-existence of a knickpoint favouring the dam location. Examples of this are the artificial dam of S2 or the highest one of S6, whereby the location on the χ plot fits with the values range of the knickpoints.
As can be observed in Fig. 9, only S2 and, to some extent, S6 networks show a strong consistency between the probability of having knickpoints and the actual location of a robust number of knickpoints. Both S3 and S4 show peaks of density values above the average. However, there is considerable uncertainty surrounding these results because of the few knickpoints located in the peaks of the χ value. Instead, the intensity peaks of S1 and S5 are highly distributed and lower than the average. In detail, S1 shows values slightly higher in both the lower and in the upper parts of the basins, while S5 is affected by greater uncertainty and does not show any outstanding density peak of expected knickpoints. The notable difference between the actual and expected knickpoint patterns, especially in S1 and S5, will be analysed in Sect. 7.
7.1 Geomorphic response to tectonic uplift
As described in Sect. 4, the Pliocene and onwards relief rejuvenation in our study area may be inferred from both the interpretation of observed geomorphological features and the results yielded by the applied quantitative methods. In addition, our structural results suggest that the distribution of such rejuvenated relief is greatly controlled by the position and orientation of two main fault systems with Quaternary activity.
The activity of overall WSW–ENE faults has strongly contributed to the roughly NNW–SSE relief segmentation of the foreland, which is particularly localised along the topographic escarpment separating Sierra Morena from the Guadalquivir foreland basin. The existence of both relict surface remnants and Neogene outcrops along the top of the escarpment has allowed us to compare the relative uplift accommodated along this escarpment and its variations from east to west.
In this regard, the foreland escarpment north of Córdoba is particularly high and exhibits a higher topographic gradient in comparison to other sectors located to the west. In this eastern sector, faulting also appears to be related to the recent northwestward tilting of the relict peneplain surface in the Guadiato river lower course (S6), which was assumed to be originally dipping towards the foreland basin. This uplift-related tilting explains the sharp stream elbow testifying to the piracy of the Guadiato river, whereby the abandoned lowermost course has remained as a wind gap.
As stated previously, well-developed debris facies colluvium is deposited at the foot of this escarpment post-dating the ancient city of Medina Azahara. Thus, this debris accumulation points to the instability of the escarpment (e.g. Forman et al., 1991) over the last 1000 years. The thickness of such colluvium is similar to that reported for recent, even active, faults (e.g. Koukouvelas et al., 2005). This recent activity is in line with some historical earthquakes recorded in Córdoba at the end of the 10th century (https://iagpds.ugr.es last access: 21 October 2022; Andalusian Institute of Geophysics and Seismic Disaster Prevention Centre, 2022). In this regard, a recent archaeological and seismological study on Medina Azahara describes oriented damages, compatible with NW–SE-oriented ground motion, which could be reasonably related to the destruction of the city at the beginning of the 11th century (Rodríguez-Pascua et al., 2021).
Towards the west, the N–S segmentation of southern Sierra Morena is still observed; however, the topographic escarpment becomes lower and less sharp. In contrast, relief rejuvenation seems to be particularly localised along the NW–SE-oriented Permian Viar basin limits, particularly along the VFS, where the fault trace coincides with the abrupt escarpment separating the Permian Viar basin and the OMZ.
This outstanding WSW–ENE topographic segmentation across the Permian Viar basin is also characterised by the topographic discontinuity of the erosional relict surface, which is located at a higher altitude on the NE side of the basin (the hanging wall of the VFS; Fig. 2b). Given that the Miocene age is attributed to such a relict surface, this discontinuity is in agreement with a Pliocene or Quaternary activity of the VFS, which uplifted the OMZ. Furthermore, the distribution of the Neogene sediments along the SE limit of the Permian Viar basin, together with the lack of said sediments in the basin, point to the same conclusion. Thus, whereas the floor of the Viar drainage basin is currently at the same altitude as the northernmost Neogene outcrops of the Guadalquivir basin, these sediments do not extend into the Viar drainage basin. This may indicate that the uplift of the forebulge region (i.e. Sierra Morena), likely accommodated in part by the WSW–ENE fault system, was prior to the River Viar drainage basin downthrow, suggesting that the VFS reactivation is relatively young within the relief rejuvenation event in Sierra Morena.
Thus, although there is qualitative and quantitative evidence of recent tectonics in the whole study area, the activity seems to be particularly manifested in sectors where basins S2 and S6 developed. The same conclusion is suggested by the comparison between the χ plots obtained for basins S1 to S6. In this regard, S2 and, to some extent, S6 show a greater consistency between the non-parametric dependence model and the current positions of knickpoints. In these basins, most of the knickpoints cluster in low χ values, thus pointing to the recent propagation of the perturbation from its source, i.e. faults located in the escarpments of Sierra Morena (S6) and the VFS (S2).
In Fig. 10, the elevation of knickpoints and dams has been plotted in χ horizontal coordinates, and the best linear fits and related regression coefficients have been calculated for basins S1 to S6. Since there are not strong lithological contrasts in the study area, we can assume that the slope of plots can be interpreted as a proxy for the tectonic activity. Thus, S6 and S2 show the greatest uplift. The others show a moderately high slope that could be also related to tectonic activity. It is worth noting that the S6 and S2 plot slopes would become steeper if those knickpoints in higher χ values, disconnected from the main clusters, were removed. In addition, the quality of their regression coefficients would increase, given that the scarce knickpoints in the upper part of the plot hamper an optimal linear interpolation. In any case, the slopes of plots for S2 and S6 suggest that these basins are located in sectors with the greatest and most recent uplift within our study area.
Moreover, only S2 and S6 are characterised by a certain consistency between observed and predicted knickpoints. Conversely, the others deviated from the obtained model. The reason for this deviation could lie in processes related to divide network reorganisation, which have been proven to alter the upstream propagation of knickpoints (Schwanghart and Scherler, 2020). In this regard, the DAI metric sized by divide order (Fig. 11) reveals significant drainage reorganisation and enables the divide migration direction to be inferred.
Such reorganisation alters drainage areas and discharge, and thus impacts on knickpoint celerities, which in return will result in more scattered knickpoint locations (Schwanghart and Scherler, 2020). Specifically, S1 is affected by a strong internal divide migration towards the east, suggesting that the western reach of S1 may have captured the eastern reach.
Moreover, the main basin divide is also moving, decreasing the basin drainage area, likely affecting the locations of the upper reach knickpoints. The SE sector of the divide between S2 and S5 is moving southwestward, thus decreasing the drainage area of the former, whereas the NW sector of the S2 divide is moving towards NW, thus increasing its drainage area. The large uncertainties around the single knickpoints occurring higher up in the drainage basin can be explained by such a drainage reorganisation. Nevertheless, S2 is experiencing a great stability that explains the strong consistency between the observed and expected knickpoint patterns in the lower part of the basin. S5 divides seem to be migrating southwestwards, gaining area from S2 and S4 and losing area in the lower part of the drainage basin along the S5–S6 main divide and, also, along minor divides. Nevertheless, in the upper part of the same divide, northeastward migration is occurring, which, combined with the aforementioned southwestward migration of the lower basin, gives rise to a clockwise rotation of the divide. Such movement will likely cause S6 to lose area at the higher part of the basin. This divide reorganisation could account for the difference in consistency among the model and the current knickpoint locations in S5 and S6. Specifically, the uncertainty and lower-than-average intensity peaks shown by the χ space profile of S5 (Fig. 9j) can be explained by such a drainage reorganisation. In S6, both the stream piracy and the wind gap formation (Figs. 4a and 11b and c) seem to be associated with the scattered knickpoint distribution. They developed linked to the uplift and northwestward tilting of the southeasternmost sector of S6. This process triggered the northwestward migration of the SE divide with the highest DAI values (Fig. 11b and c), which is still ongoing in the sector where the fault-related escarpment changes orientation from WSW–ENE and SSW to NNE. Although the divide reorganisation provides an explanation for the scattered distribution of knickpoints, the reason may be also related to the strain partitioning expected in a region widely affected by previous mechanical discontinuities. Indeed, knickpoints originating from the same perturbation (e.g. a single event in a single fault) must cluster on a χ space profile. This situation happens in S2, where deformation is very localised by a discrete fault system (VFS), which is here interpreted as a reactivated major Variscan tectonic contact. However, in the rest of our study area, the recent deformation does not seem to be accommodated by major faults but rather highly partitioned into distributed, variably oriented faults. Thus, several perturbations that originated in different faults could be superimposed along the stream network, and therefore, knickpoints would not cluster. In this regard, this geomorphic tool could be useful to test the localisation versus the distribution of the strain.
7.2 Matching the geomorphic results with the tectonic scenario
The Sierra Morena is characterised by significant mechanical discontinuities achieved during its complex tectonic evolution. These discontinuities are predominantly defined by both NW–SE-oriented Variscan structures and, mainly, WSW–ENE faults related to the Alpine orogenic cycle, which eventually gave rise to the Betic Chain building during Neogene times. Such orientations coincide with those found for faults with Quaternary activity, thus suggesting that the observed relief rejuvenation pattern is strongly determined by the reactivation of previous structures that are accommodating the current strain partitioning.
The overall WSW–ENE trend of faults associated with the Sierra Morena southern escarpment, and in general to its NNW–SSE relief segmentation, is in agreement with those expected to accommodate extension by flexural bending in the Betic forebulge, i.e. parallel to this topographic high. In this regard, normal faults with a dominant dip–slip component, therefore producing extension roughly orthogonal to the forebulge trend, are frequent. Nevertheless, the overall cartographic WSW–ENE trend of the escarpment is at a smaller scale, defined by faults whose orientations range from SW–NE to WNW–ESE. This suggests that not only newly formed forebulge-related faults may be involved but also those Variscan structures with an orientation that favoured their reactivation. Examples of Variscan WNW–ESE structures recently reactivated as normal faults have been previously described in the Sierra Albarrana area (SA in Fig. 1c; Herraiz et al., 1996). Additionally, reactivated late Variscan SW–NE to WSW–ENE fractures also seem to be present. Examples include joints exhibiting striated surfaces in late Paleozoic igneous rocks or the Embalse del Cala fault (Figs. 2a and 3c), which is a left-lateral fault (García-Navarro and Fernández, 2004) interpreted in this work as being a reactivated normal dextral fault.
Although most of these structures have a normal slip component, many of them are roughly vertical or even steeply dipping reverse faults, suggesting that the current vertical extrusion is significant in the forebulge zone. This may indicate that compression is tightening this flexural relief, also explaining the reactivation of the Variscan NW–SE-oriented VFS as a shortening structure. This tightening is consistent with previous seismotectonic analysis in Sierra Morena, showing that focal mechanisms of reverse faults are deeper than those of normal faults (Herraiz et al., 1996). This vertical distribution of the stress matches with tangential longitudinal strain by lithospheric buckling. In this respect, previous numerical models of the paired Betic foreland basin–forebulge (i.e. Guadalquivir basin/Sierra Morena) evolution have settled that the current altitude of Sierra Morena cannot be explained only by lithospheric flexure of the South Iberian basement. Therefore, these models invoke compressional tectonic forces to enhance the Sierra Morena uplift by lithospheric folding (García-Castellanos et al., 2002; Cloething et al., 2002). This is in line with the amplitude/width ratio of Sierra Morena, which is significantly higher than other forebulge examples (e.g. Niviere et al., 2013).
This compressional setting has often been contextualised within the overall NW–SE-oriented compression of the Iberian Peninsula, which is linked to the convergence between the Eurasian and the African plates (e.g. Herraiz et al., 2000, and references therein). Nevertheless, this NW–SE-oriented compression hardly explains either the dextral component that is frequently exhibited by the WSW–ENE fault system or the reverse slip accommodated by the VFS, which is oriented parallel to this compression direction. In this respect, our results seem to be more compatible with forebulge compression due to the intraplate propagation of the Betic transpressional deformation front. Indeed, the Neogene to recent dextral transpressional kinematics recorded in segments of the western Betics is consistent with a N99∘ E–N109∘ E trending horizontal velocity vector (Díaz-Azpiroz et al., 2014; Barcos et al., 2015, 2016) attributed to the westward migration of the western Gibraltar Arc (Balanyá et al., 2012; Gutscher et al., 2002). This shortening orientation would have reactivated the VFS as a left-lateral reverse fault. Additionally, the dextral transpressional deformation of the forebulge would generate a SW–NE-oriented extension. This extension would imprint overall dextral kinematics on the WSW–ENE to WNW–ESE faults, which would be characterised by a high strain partitioning due to the different orientation of the reactivated structures. Interestingly, fault population analysis techniques applied to sectors nearby our study area have yielded a similar SW–NE-oriented extension (Smin trend; Herraiz et al., 2000).
Our results show that the combination of geomorphological and structural analyses of ancient areas can be a powerful tool to not only explore the role of reactivated structures on relief rejuvenation but also to delve into the tectonic setting responsible for such a reactivation. This combined analysis can be exported to any long-lived region in order to compare the proposed tectonic setting with the observed geomorphological features. In our case, we have interpreted, in tectonic terms, the main geomorphological traits of Sierra Morena, which is a flexural relief (i.e. the forebulge) generated in the Betic foreland due to the load exerted by the orogenic pile.
The analysed drainage network of Sierra Morena shows a wide range of relief rejuvenation signs such as (i) preserved relicts of a Miocene peneplain, shaped at the foreland basin base level and now located several hundreds of metres above it (this peneplain is, in places, stepped and/or tilted), (ii) incised meanders, fault-related streams deflection, and stream piracy, and (iii) patches of shallow-water marine Miocene deposits (now at different altitudes up to 400 m a.s.l). These elements, taken together, give rise to a topography of flat-lying interfluves, often constituted by either patches of Miocene rocks or remnants of the Miocene peneplain, deeply incised by the drainage network.
The qualitative geomorphological characterisation together with the use of geomorphic indices evidence the relationship between mountain fronts and Quaternary activity of both newly formed and reactivated faults. The main faults controlling relief rejuvenation belong to two different groups. The first is mainly composed of WSW–ENE, right-lateral normal faults responsible for the NNW–SSE relief segmentation of Sierra Morena and the abrupt escarpment between this range and the Guadalquivir foreland basin. The other fault group is localised on the Viar fault system (VFS), previously interpreted as a late Variscan left-lateral reverse fault system, and is responsible for WSW–ENE relief segmentation in the western sector of the study area.
Knickpoint pattern modelling, based on χ space and performed on six drainage basins, enables us to define the relationship between the activity of the analysed structures and the current geomorphological features of Sierra Morena in a more precise manner. The main stems of these selected basins are crosscut by fault segments, which are related to either the Sierra Morena southern escarpment or the reactivated VFS. The planimetric and altimetric knickpoints clustering on χ profiles confirms that the faults located in the Sierra Morena southern escarpment have experienced recent, although somehow diachronous, tectonic activity. Our analysis also evidences differences in relative uplift along this escarpment. Moreover, divide migration controls the deviation observed between modelled and observed knickpoint distribution, as indicated by the computed values of the divide asymmetry index (DAI).
On the whole, our results deviate from those expected in a typical flexural forebulge. In addition to flexural-related deformation, the kinematic features of faults related to the current Sierra Morena relief point to the Quaternary, strongly partitioned, transpressional deformation of the Betic foreland. This is compatible with the intraplate propagation of the Betic fold and thrust deformation.
Codes rely on TopoToolbox (Schwanghart and Scherler, 2014), which is freely available at https://topotoolbox.wordpress.com/download (Schwanghart, 2014).
TanDEM-X data were kindly provided by the German Aerospace Center (Wessel, 2016; DLR; project ID: DEM_HYDR3360; https://tandemx-science.dlr.de; German Aerospace Center, 2016).
The software used for stereoplots is FaultKin (Richard W. Allmendinger © 2020–2022), which is freely available at https://www.rickallmendinger.net/faultkin (Allmendinger, 2019).
IE led the research and wrote the draft. AJB and MD made the quantitative geomorphological analyses. IE, AJB, JLY, JCB, and FM participated in the fieldwork for both qualitative geomorphological analysis and structural analysis. All the authors participated in the results interpretation and in the text improvement.
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 thank the editor, Niels Hovius, and the associate editor, Richard Gloaguen. We also appreciate the thorough review of Stefan Hergarten and Colin P. Stark, whose comments significantly improved this article.
This research is part of the project PGC2018-100914-B-I00, funded by the Ministerio de Ciencia e Innovacíon (Spanish Government)/AEI/10.13039/501100011033/ERDF, and the project UPO-1259543, funded by the Consejería de Economía, Conocimiento, Compañías y Universidad (Andalusian Government)/ERDF.
This paper was edited by Richard Gloaguen and reviewed by Stefan Hergarten and C. P. Stark.
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