Nouvelles donnéessur le Paléocène-Éocène des zones internes bético-rifaines

Maaté, Alí; Martín‐Algarra, Agustín; Martı́n-Martı́n, Manuél; Serra‐Kiel, Josep

doi:10.1016/s0016-6995(00)80074-1

Cited by 16 publications

(16 citation statements)

References 2 publications

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“…Tectonics DAUDET ET AL. transgression is outlined by the deposition of 10-20 m of shallow-marine carbonaceous platform unconformably overlying the late Cretaceous deposits and established over all the Malaguide Complex from the Late Ypresian, 52-50 Ma (Hanne et al, 2003;Lonergan & Mange-Rajetzky, 1994;Maaté et al, 2000). Field data in the Prebetic also agree with a transgression in late Thanetian (56 Ma) to late Ypresian (50 Ma) as shown by the development of a turbiditic basin (Martín-Chivelet & Chacón, 2007) that they interpret to reflect the initiation of Africa-Europe convergence.…”

Section: 1029/2020tc006093mentioning

confidence: 68%

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Tectono‐Stratigraphic and Thermal Evolution of the Western Betic Flysch: Implications for the Geodynamics of South Iberian Margin and Alboran Domain

et al. 2020

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The Betic‐Rif orogen is a key region to understand the evolution of the plate boundary between Africa and Iberia/Europe. This study focuses on the Flysch Complex, which is considered the sedimentary cover of a domain originally positioned between the Iberian and Alboran margins. Based on stratigraphic and depositional evolution constraints, evidence for salt tectonics, combined with new apatite fission‐tracks (AFT) and (U‐Th‐Sm)/He ages from the Flysch Complex and the Subbetic Zone, we propose a geodynamic interpretation for the formation of the Betic Cordillera, accounting for moderate N‐directed transport of the Flysch Complex and synchronous exhumation between External and Internal Zones of the Betic. Early contraction between Africa and Iberia/Europe is reflected in the Cretaceous Flysch basin by a prolonged period of residence in the partial annealing zone for AFT and onset of foreland subsidence at 50 Ma. This stage lasted until the Early to Middle Miocene (20–15 Ma), marked by the rapid succession, in less than 5 Ma, of the deposition of Cenozoic flysch and their rapid exhumation. This event is interpreted to reflect the W‐directed retreating mantle delamination between Africa and Iberia margins at the origin of the collapse of the proto‐Betic orogenic domain and formation of the Alboran domain.

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Section: 1029/2020tc006093mentioning

confidence: 68%

“…Martín-Algarra). They are followed unconformably by Eocene calcareous turbidites with alveolines and numulites ( Figure 4) (Guerrera et al, 2006;Maaté et al, 2000;Martín-Martín et al 1997;Serrano et al, 1995;Serra-Kiel et al, 1998) that witness the initiation of the foreland subsidence and therefore collision. Hanne et al (2003).…”

Section: 1029/2020tc006093mentioning

confidence: 99%

Tectono‐Stratigraphic and Thermal Evolution of the Western Betic Flysch: Implications for the Geodynamics of South Iberian Margin and Alboran Domain

et al. 2020

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“…As the latter is unlikely to reach the extension and thickness of SU1 (given the limited shape of the Maghrebian flysch klippe onshore), we opt for the Ghomaride complex. The Ghomaride unit is the topmost nappe composing the Alboran domain and mainly consist of slightly metamorphic Paleozoic successions (Chalouan, 1986) (Chalouan and Michard, 1990;Maaté et al, 2000;El Kadiri et al, 2006;Martín-Martín et al, 2006). The Ghomaride unit is separated from the Alpujarride-Sebtide by an extensional detachment (Chalouan and Michard, 1990).…”

Section: Accepted Manuscriptmentioning

confidence: 99%

Tectonic and stratigraphic evolution of the Western Alboran Sea Basin in the last 25 Myrs

et al. 2016

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“…After the HT metamorphic episode (~23 -21 Ma) and exhumation, non-deposition and erosion during the 'Aquitanian Paroxysm', early Burdigalian strata (yielding the first detritus of Sebtide Complex provenance) onlapped early Aquitanian deposits in the Tetouan-Martil Basin with an angular unconformity (OuazaniTouhami & Chalouan, 1995). This unconformity indicates tectonic uplift and thrusting of Internal Rif nappes (Maate et al, 1995). Regionally, both formations record a succession of Netherlands Journal of Geosciences -Geologie en Mijnbouw | 87 -4 | 2008 266 three extensional phases: NE-SW to NNE-SSW rifting in the late Chattian, NW-SE to NNW-SSE extension during the Aquitanian and ENE-WSW to E-W extension in the early Burdigalian (Ouazani-Touhami & Chalouan, 1995;Zaghloul et al, 2003).…”

Section: Rif Basins (Figs 4 8; Appendices 1 -7)mentioning

confidence: 99%

“…The mountain ranges of the Internal Rif Domain emerged and collapsed during Late Oligocene-Miocene rifting and low-angle normal faulting. Eventually, the Alboran terrane was transformed in the early-middle Tortonian into marine basins by tectonic subsidence governed by NNE-SSW to ENE-WSW compression (Chalouan et al, 1995(Chalouan et al, , 1997(Chalouan et al, , 2001 Benmakhlouf & Chalouan, 1995; Aït Brahim et al, 2002).The oldest syn-rift deposits of the northern Internal Rif belong to the Fnideq Formation (late Chattian-early Aquitanian) and 'Viñuela Formation' (early Burdigalian) near Ceuta (El Kadiri et al, 2000), the type Fnideq Formation at Fnideq (overthrust by Numidian turbidite sandstones; Feinberg et al, 1990;Ouazani-Touhami & Chalouan, 1995), and the Fnideq Formation and Sidi Abdeslam Formation (early Burdigalian) in the Tetouan-Martil Basin, a quadrangular depocentre that opened by NE-SW extension at the end of the Oligocene (Feinberg et al, 1990; Benmakhlouf & Chalouan, 1995;Maate et al, 1995;Ouazani-Touhami & Chalouan, 1995). These molassic strata regionally transgressed the block-faulted Ghomaride Complex (the highest tectonic element of the Rif) with high-density turbidity currents depositing clastics in a network of small 'basins' with subsidence governed by normal faulting (Zaghloul et al, 2003).…”

mentioning

confidence: 99%

Punctuated Neogene tectonics and stratigraphy of the African-Iberian plate-boundary zone: concurrent development of Betic-Rif basins (southern Spain, northern Morocco)

Sissingh

2008

Netherlands Journal of Geosciences

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The geological configuration of the present-day Mediterranean is characterized by a complex and extensive system of both interconnected and fragmented fold-and thrust belts that is associated with back-arc basins (e.g. Carminati et al., 1998;Rosenbaum & Lister, 2004). Their tectonic structure and setting are varied, and the compressional origin and growth of the different belts and the formation of the adjoining extensional basins also varies considerably in age. The different fold-andthrusts belts did not evolve during one single, uninterrupted cycle of Alpine orogenesis, but are the ultimate outcome of a prolonged, polyphase process of intermittent plate-tectonic interaction between the African-Arabian and Eurasian plates. This resulted in the creation and ultimate disappearance of two major oceanic basins, the Palaeotethys (mainly Palaeozoic) and the Neotethys (late Palaeozoic-Mesozoic). As in the preceding Jurassic and Cretaceous times, the motions of Africa-Arabia relative to Eurasia during the Tertiary were an important control on the geological evolution of the Alpine Tethys (late Mesozoic-Tertiary). Various kinematic frameworks for palaeotectonic and palaeogeographic reconstructions have been proposed for the region (e.g. Dewey et al., 1989;Rosenbaum et al., 2002). These were mostly based on analysis of rotation parameters (poles of rotation, rotation angles), which allowed to constrain past relative velocities between Africa and Eurasia. In addition, analysis of North Atlantic magnetic lineations helped to constrain the movement of Africa and Europe relative to North America. The consensus view is that during the Late Cretaceous Africa converged towards Europe in a S-N directed rotational mode. This was contemporaneous with spreading of the Azores part of the North Atlantic, the coeval opening of the Gulf of Biscay like a sphenochasm and the resulting anti-clockwise rotation of Iberia with respect to Eurasia. Sinistral motion occurred after an active plate boundary subject to left-lateral strike-slip faulting had been established at the northern margin of the Iberian block. Consequently, Iberia behaved like a promontory AbstractThis paper integrates the sequence stratigraphic and tectonic data related to the Neogene geodynamic and palaeogeographic development of the African-Iberian plate boundary zone between Spain and Morocco. Though the dating of individual tectonostratigraphic sequences and their delimiting sequence boundaries varies in accuracy and precision, their apparent correlation strongly suggests contemporaneous development of the Betic and Rif basins. This may likely be attributed to regional changes of the overall compressional intra-plate stress field. This, in turn, was governed by coeval plate-kinematic changes related to the ongoing collisional convergence of Africa and Iberia. The Neogene succession is characterised by brief tectonic pulses that governed the sequence stratigraphic development of the Betic-Rif basins (NBR phases). It broadly correlates with the coeval sequences in the ...

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Nouvelles donnéessur le Paléocène-Éocène des zones internes bético-rifaines

Cited by 16 publications

References 2 publications

Tectono‐Stratigraphic and Thermal Evolution of the Western Betic Flysch: Implications for the Geodynamics of South Iberian Margin and Alboran Domain

Tectono‐Stratigraphic and Thermal Evolution of the Western Betic Flysch: Implications for the Geodynamics of South Iberian Margin and Alboran Domain

Tectonic and stratigraphic evolution of the Western Alboran Sea Basin in the last 25 Myrs

Punctuated Neogene tectonics and stratigraphy of the African-Iberian plate-boundary zone: concurrent development of Betic-Rif basins (southern Spain, northern Morocco)

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