Topography and palaeogeographic evolution of a middle Miocene foredeep basin plain (Northern Apennines, Italy)

Lucente, C. C.

doi:10.1016/j.sedgeo.2004.06.002

Cited by 37 publications

(57 citation statements)

References 29 publications

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“…La sédimentation des bassins piggyback est syntectonique (Parish, 1984;Williams, 1985;Roure et al, 1990;Cojan et Renard, 1997;Clift et al, 2004;Lucente, 2004;Sepehr et Cosgrove, 2004). La concentration de la déformation dans la zone de collision mène à un soulèvement rapide et l'érosion résulte à l'accumulation d'une énorme charge sédimentaire Coney, 1973;Crittenden et al, 1980).…”

Section: 222-relation Entre Tectonisme Et Sédimentation Dans Les unclassified

“…Discordances intra-bassins, interdigitation, cyclicité, variations latérales et verticales de faciès (impliquant granocroissance, cycles positifs et négatifs, amincissement et épaississement des lits de grès) et migrations des aires de dépôts, sont interprétées comme une influence des processus allocycliques comme le tectonisme, le volcanisme, le climat et la variation de la topographie (Lucente, 2004). Des séquences cycliques sont associées à l'influence des facteurs allocycliques sur la sédimentation (Edwards et al, 2005;Eriksson et al, 2001;Hall et al, 2005;Hein, 1987;Hunter and Clifton, 1982;Martins-Neto et al, 2001;Mishra et al, 2004;Mueller et al, 1994).…”

Section: 22-changements Latéraux Et Verticaux De Facièsunclassified

“…Dans ce milieu, les dépôts progradent du bassin profond à un prodelta, un front de delta puis à une plaine deltaïque. Les empilements épais Les plis isoclinaux, serrés et renversés sont des structures communes aux bassins piggyback (de Wit, 1982;Lucchi, 1990;Lucente, 2004;Parish, 1984). Les plis asymétriques constituent une manifestation en surface de structures associées à un décollement (Li et al, 2009).…”

Section: 4-modèle Paléogéographique Et Tectoniqueunclassified

“…La nature des fragments dépend également de celle du réservoir magmatique sous-jacent aux failles. Tout comme pour les bassins de décrochement, la sédimentation est synchrone au tectonisme; la déformation affectant les sédiments a lieu lors de leurs dépôts (Parish, 1984;Williams, 1985;Roure et al, 1990;de Wit, 1991 ;Clift et al, 2004;Lucente, 2004;Sepehr et Cosgrove, 2004). La largeur n'excède pas quelques dizaines de km ( …”

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“…Les sédiments les plus anciens sont typiquement d'eau profonde, communément la section stratigraphique est condensée, ce qui dénote qu'elle est privée de sédiments (Miall, 1995). Les bassins piggyback décrits dans la littérature sont synthétisés au tableau 1-3 (Clift et al, 2004;Cojan et Renard, 1997;de Wit, 1982de Wit, , 1991Débelmas et Mascle, 1991;Dewey, 1969;Dewey et Bird, 1970;Dewey et al, 1986;Evans, 1994; Kusky et Veancombe, 1997;Leeder et Gawthorpe, 1987;Lucchi, 1990;Lucchitta, 1990;Lucente, 2004;Mellerea et al, 2005;Miall, 1995;Muoz et al, 1986;Ori et Friends, 1984;Parish, 1984;Puigdefabregas et al, 1986;Roure et al, 1990;Sepehr et Cosgrove, 2004;Williams, 1985). …”

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Caractéristiques sédimentologiques, volcanologiques et structurales du bassin de Granada dans la ceinture de roches vertes de l'Abitibi (Québec) /

Diop¹

2011

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The Granada Basin, correspond to the stratigraphie unit known as the Granada Formation. This unit lies in the southernmost part of the Southern Volcanic Zone of the greenstone dominated Abitibi Subprovince in Quebec.Faciès analysis in the Granada Basin has identified clastic and volcaniclastic rocks deposited in an environment evolving from relatively deep marine to fluvial. The earliest sediments were mainly turbidites (faciès la and lb) deposited in extensional sub-basins. These sediments were overlain by a regressive sequence that evolved from shallow marine wave base dominated sediments (faciès 2a) to coastal deposits (faciès 2b). These deposits represent the transition between marine and continental depositional environments. The transition zone is marked by deposits of sandstoneargillites-stratified pebble conglomerate (faciès 2b) transported by waves and tides between the subtidal and intertidal zone. Faciès 3a and 3b of the felsic volcaniclastic lithofacies are interbedded with faciès la, lb and 2a.Deposits of the Granada Basin are transitional faciès separated by intra-basin unconformities, which are characteristic of sedimentary basins formed along fault margins. The volcano-sedimentary deposits of the Granada Basin have characteristics of sedimentation influenced by tectonisme such as: i) local and basinwide lateral and vertical faciès variations; ii) alternating fining and coarsening upwards sequences; iii) high rate of accumulation of sediments; iv) some conglomerate boulders are over 1 m in size and the thickness of conglomerate deposits; v) interdigitation of conglomerates and sandstones that denotes a progradation; vi) intra-basin unconformities; vii) the local source of conglomerates; and viii) associated alkaline magmatism. Tectonism would be ongoing throughout the development of the basin which would have induced several phases of source renewal areas for the sediments coupled with intra-basin unconformities. The earliest formed sedimentary deposits of the Granada Basin were affected by uplift and subsequently eroded and recycled into later basin fill along intra-basin unconformities. Gradually as the basin filled the sedimentary deposits became less and less shallower which is a characteristic of piggyback-type basins. The decrease in the depth is a consequence of an increase in topography due to repeated uplift along faults.Sedimentary rocks of the Granada Basin were intruded by alkalic mature volcanic arc-type sills, stocks and porphyritic dikes. These intrusive rocks are similar to Timiskaming-type porphyry intrusions and volcanic rocks found in the Kirkland Lake area of Ontario.The structural style of the Granada Basin, consisting of overturned southward verging tight to isoclinal folds, is characteristic of thrust basins. Two major east-west trending synclinal axial traces are distinguishable and their juxtaposition in a back to back relationship is compatible with there being an unconformity between them. This unconformity is further demonstrated by the presence of sandstone cla...

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Section: 222-relation Entre Tectonisme Et Sédimentation Dans Les unclassified

Section: 22-changements Latéraux Et Verticaux De Facièsunclassified

Section: 4-modèle Paléogéographique Et Tectoniqueunclassified

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Caractéristiques sédimentologiques, volcanologiques et structurales du bassin de Granada dans la ceinture de roches vertes de l'Abitibi (Québec) /

Diop¹

2011

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Mass‐Transport Complexes of the Marnoso‐arenacea Foredeep Turbidite System (Northern Apennines, Italy)

Pini

Lucente

Venturi

et al. 2019

Submarine Landslides

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Tectonics of Sedimentary Basins, with Revised Nomenclature

Ingersoll

2011

Tectonics of Sedimentary Basins

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Actualistic plate-tectonic models are the best framework within which to understand the tectonics of sedimentary basins. Sedimentary basins develop in divergent, intraplate, convergent, transform, hybrid, and miscellaneous settings. Within each setting are several variants, dependent on type(s) of underlying crust, structural position, sediment supply, and inheritance. Subsidence of sedimentary basins results from (1) thinning of crust (2) thickening of mantle lithosphere (3) sedimentary and volcanic loading (4) tectonic loading (5) subcrustal loading (6) asthenospheric flow, and (7) crustal densification. Basins vary greatly in size, life span, and preservation potential, with short-lived basins formed in active tectonic settings, especially on oceanic crust, having low preservation potential, and long-lived basins formed in intraplate settings having the highest preservation potential.Continental rifts may evolve into nascent ocean basins, which commonly evolve into active ocean basins bordered by intraplate continental margins with three types of configurations: shelf-slope-rise, transform, and embankment. Continental rifts that do not evolve into oceans become fossil rifts, which later become sites for development of intracratonic basins and aulacogens. If all plate boundaries within and around an ocean basin become inactive, a dormant ocean basin develops, underlain by oceanic crust and surrounded by continental crust.Sites for sedimentary basins in convergent settings include trenches, trench slopes, forearcs, intra-arcs, backarcs, and retroarcs. Complex dynamic behavior of arc-trench systems results in diverse configurations for arc-related basins. Most notable is the overall stress regime of the arc-trench system, with resulting response along and behind the magmatic arc. Intra-arc rifting in highly extensional arcs commonly evolves into backarc spreading to form new oceanic crust. Backarcs of neutral arcs can contain any type of preexisting crust that was trapped there at the time of initiation of the related subduction zone. Highly compressional arcs develop retroarc foldthrust belts and related retroforeland basins, and may develop hinterland basins; in extreme cases, broken retroforelands may develop in former cratonal areas.As nonsubductable continental or arc crust is carried toward a subduction zone, collision generally initiates at one point and the resulting suture propagates away from this point of initial impact. Remnant ocean basins form on both sides of the initial impact point, and rapidly fill with sediment derived from the suture zone. As collision continues, the flux of sediment into the remnant ocean basin(s) increases concurrently with shrinkage of the basin until final suturing and obduction of the accreted sediment occur. Concurrently with collision, proforeland basins form on continental crust of the subducting plate and collisional retroforeland basins form on the overriding plate. Impactogens, broken forelands, and hinterland basins also may result.In transform settings and along c...

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Topography and palaeogeographic evolution of a middle Miocene foredeep basin plain (Northern Apennines, Italy)

Cited by 37 publications

References 29 publications

Caractéristiques sédimentologiques, volcanologiques et structurales du bassin de Granada dans la ceinture de roches vertes de l'Abitibi (Québec) /

Caractéristiques sédimentologiques, volcanologiques et structurales du bassin de Granada dans la ceinture de roches vertes de l'Abitibi (Québec) /

Mass‐Transport Complexes of the Marnoso‐arenacea Foredeep Turbidite System (Northern Apennines, Italy)

Tectonics of Sedimentary Basins, with Revised Nomenclature

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