Turbidite facies, fluid-escape structures and mechanisms of emplacement of the Oligo-Miocene Aljibe Flysch, Gibraltar Arc, Betics, southern Spain

Stromberg, S. G.; Bluck, B. J.

doi:10.1016/s0037-0738(97)00096-1

Cited by 22 publications

(19 citation statements)

References 20 publications

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“…They overly Chattian Beneiza Flysch with a pronounced change in lithofacies from thin-bedded, marly sandstones to thick-bedded, massive sandstones. This contact that is interpreted as a major, non-erosional sequence boundary separating two different depositional systems at the Chattian-Aquitanian transition (Stromberg & Bluck, 1998). The upper part of the Aljibe flysch consists of late/middle Burdigalian sandstones and siltstones referred to as the Neonumidian Formation (López-Garrido & Sanz de .…”

Section: Tectonostratigraphy Of Betic Basins (Figs 4 -6; Appendices 1mentioning

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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Section: Tectonostratigraphy Of Betic Basins (Figs 4 -6; Appendices 1mentioning

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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“…Such associations are partly different from the succession of the Oligo-Miocene Aljibe Flysch in southern Spain described by Stromberg & Bluck (1998). The ideal sequence of events leading to the formation of water-escape structures described by these authors begins with a coarse-grained sandstone with or without convolutions, that passes into dark laminae and/or dish structures, followed by closely to widely spaced vertical tubes, inclined tubes, sills and pillars, and, finally, sand volcanoes.…”

Section: Discussionmentioning

confidence: 73%

Soft-sediment deformation structures in seismically affected deep-sea Miocene turbidites (Cilento Basin, southern Italy)

2014

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Soft-sediment deformation structures (SSDS) are widespread in the upper part of the S. Mauro Formation (Cilento Group, Middle-Late Miocene). The succession is represented mainly by thick and very thick, massive, coarse-grained sandstones, deposited by rapid sedimentation of high-density turbidity currents. The most common SSDS are short pillars, dishes, sedimentary sills and convolutions. They occur mostly in the upper parts of sandstone beds. Vertical tubes of 4-5 cm in diameter and up to 50 cm long constitute the most striking structures. They begin in the middle part of sandstone beds, which are basically massive or contain faint dish structures. These tubes can bifurcate upwards and/ or pass into bedding-parallel veins or dikes. The vertical tubes sometimes form sand volcanoes on the then sedimentary surface. The SSDS are interpreted as the result of earthquake-triggered liquefaction and/or fluidisation of the turbidites that were affected by the seismic shocks. This implies that the deformed layers should be considered as seismites.

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“…In the Sm-1 borehole, most of these factors are related to density flows such as turbidite flows, where the presence of a slope is presumed. Soft-sediment deformation structures, such as load casts, ball-andpillow structures, convolute lamination, and water-escape structures and dewatering, have been recognized as common parts of turbidite successions (Dzulynski and Walton 1965;Ricci Lucchi 1995;Wallis 1969;Lowe 1982;Guy 1992;Stromberg and Bluck 1998;Haughton et al 2009;Moretti et al 2001;Sumner et al 2012). It is well known that turbidite flows produce very heterolithic successions, which impede permeability within sediment units and cause changes in pore pressure.…”

Section: Discussionmentioning

confidence: 99%

“…Field analyses and modelling on the liquefaction and fluidization processes induced by rapid sedimentation in lacustrine, delta, and offshore marine environments are often associated with turbidity currents. Dzulynski and Walton (1965), Wallis (1969), Lowe (1982), Larsen (1986), Guy (1992), Stromberg and Bluck (1998), and Moretti et al (2001) focused on understanding turbidite formation mechanisms in the laboratory. Their experiments resulted in asymmetrical pillow structure and elongated sets of load casts.…”

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confidence: 99%

Types of soft-sediment deformation structures in a lacustrine Ploužnice member (Stephanian, Gzhelian, Pennsylvanian, Bohemian Massif), their timing, and possible trigger mechanism

Stárková

Martínek

Mikuláš

et al. 2015

Int J Earth Sci (Geol Rundsch)

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facies associations preserve from 22.5 to 20.5 cm SSDS/m, and in palustrine carbonate, 13.5 cm mechanical SSDS/m was found. SSDS in fluvial facies are rare (2.9 cm SSDS/m). The distribution of SSDS in the Sm-1 borehole shows clear relationships to sedimentary facies and processes such as density flows or fluctuation of water level. The relationships of particular structures indicate a relative timing of formation which is as follows: sediment deposition was followed by the formation of mechanical SSDS, then by bioturbation, and finally by deformations due to early diagenetic growth of carbonates and silica. The distribution of SSDS in vertical sections and their direct relationship to sedimentary facies point to endogenic rather than external trigger mechanisms such as seismic activity. The main endogenic trigger mechanisms responsible for the origin of SSDS included a Stephanian semi-humid seasonal climate, basin morphology with relatively steep gradients, and elevated source areas, which created a conducive environment for rapid and repeated deposition of sheetfloods and hyperconcentrated flows and turbidites causing syndepositional loading.

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Turbidite facies, fluid-escape structures and mechanisms of emplacement of the Oligo-Miocene Aljibe Flysch, Gibraltar Arc, Betics, southern Spain

Cited by 22 publications

References 20 publications

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

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

Soft-sediment deformation structures in seismically affected deep-sea Miocene turbidites (Cilento Basin, southern Italy)

Types of soft-sediment deformation structures in a lacustrine Ploužnice member (Stephanian, Gzhelian, Pennsylvanian, Bohemian Massif), their timing, and possible trigger mechanism

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