Retroarc foreland systems––evolution through time

Catuneanu, Octavian

doi:10.1016/j.jafrearsci.2004.01.004

Cited by 166 publications

(139 citation statements)

References 36 publications

(77 reference statements)

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“…The Central Rand Group records an increasingly nonmarine affinity, and is the product of deposition in alluvial fan, fluvial and shallow marine environments. The balance between marine and nonmarine sedimentation gradually changed in favour of the latter as the basin evolved from an early underfilled phase (represented by the West Rand Group) to a late overfilled phase (represented by the Central Rand Group) (Catuneanu, 2001(Catuneanu, , 2004. At the same time, the interior seaway of the Witwatersrand Basin became progressively shallower and more restricted to the distal region of the basin as the proximal nonmarine systems prograded and replaced the marine systems through time (Tankard et al, 1982;Karpeta et al, 1991;Mayer, 1992, 1998).…”

Section: Sedimentation Within the Witwatersrand Basin S E Ns U S T R mentioning

confidence: 99%

Meso-Archaean and Palaeo-Proterozoic sedimentary sequence stratigraphy of the Kaapvaal Craton

Bumby

Eriksson

Catuneanu

et al. 2012

Marine and Petroleum Geology

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ABSTRACT:The Kaapvaal Craton hosts a number of Precambrian sedimentary successions which were deposited between 3105 Ma (Dominion Group) and 1700 Ma (Waterberg Group) Although younger Precambrian sedimentary sequences outcrop within southern Africa, they are restricted either to the margins of the Kaapvaal craton, or are underlain by orogenic belts off the edge of the craton. The basins considered in this work are those which host the Witwatersrand and Pongola, Ventersdorp, Transvaal and Waterberg strata. Many of these basins can be considered to have formed as a response to reactivation along lineaments, which had initially formed by accretion processes during the amalgamation of the craton during the Mid-Archaean.Faulting along these lineaments controlled sedimentation either directly by controlling the basin margins, or indirectly by controlling the sediment source areas.Other basins are likely to be more controlled by thermal affects associated with mantle plumes. Accommodation in all these basins may have been generated primarily by flexural tectonics, in the case of the Witwatersrand, or by a combination of extensional and thermal subsidence in the case of the Ventersdorp, Transvaal and Waterberg. Wheeler diagrams are constructed to demonstrate stratigraphic relationships within these basins at the first-and second-order levels of cyclicity, andcan be used to demonstrate the development of accommodation space on the craton through the Precambrian.

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Section: Sedimentation Within the Witwatersrand Basin S E Ns U S T R mentioning

confidence: 99%

Meso-Archaean and Palaeo-Proterozoic sedimentary sequence stratigraphy of the Kaapvaal Craton

Bumby

Eriksson

Catuneanu

et al. 2012

Marine and Petroleum Geology

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“…dynamic subsidence: Mitrovica et al 1989;Gurnis 1992;Catuneanu et al 1997;Pysklywec & Mitrovica 2000;Catuneanu 2004). Combined with orogenic supracrustal loading (load of the mountain belt exerted on the continental lithosphere), these are the primary subsidence mechanisms that control accommodation and sedimentation patterns in retro-foreland basin (DeCelles & Giles 1996;Pysklywec & Mitrovica 1999;Catuneanu 2004).…”

Section: The Amazonian Foreland Basin System 63mentioning

confidence: 99%

“…5.1;Jordan et al 1983;Jordan 1995;Horton & DeCelles 1997). Foreland basins are a favoured area for studying the interplay at different scales of tectonics, climate and sedimentation (see, e.g., Beaumont 1981;Burbank 1992;Jordan 1995;DeCelles & Giles 1996;Horton 1999;Catuneanu 2004 amongst many others) as they record the denudation of the adjacent mountain belt and hence the interaction between erosion and mountain growth. The stratigraphic record of foreland basins is generally very complete (Jordan 1995), and shortening, mountain building and the initiation of the Andean foreland basin started in Late Cretaceous-Paleocene times (Balkwill 1995;DeCelles & Horton 2003;Barragan et al 2005;Martin-Gombojav & Winkler 2008 and references therein).…”

Section: Introductionmentioning

confidence: 99%

Cenozoic Sedimentary Evolution of the Amazonian Foreland Basin System

Roddaz

Hermoza

Mora

et al. 2009

Amazonia: Landscape and Species Evolution

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In this chapter we present a synthesis of the Cenozoic evolution of the Amazonian foreland basin system, based on a review of the estimated ages, lithology and sedimentary structures, palaeontological content, and inferred depositional environments of sedimentary units in the basin. In addition, we have calculated maximum sedimentation rates for the Cenozoic formations of the northern Peruvian foreland basin and integrated these with existing data on sedimentation rates, subsidence analysis, migration of depocentre and depositional environments. Based on this information we propose a model for the Cenozoic evolution of the Amazonian foreland. The sedimentary architecture of this foreland basin indicates that Cenozoic evolution was marked by several periods, which were roughly synchronous and of similar effect, along the entire Amazonian foreland basin system. Tectonic loading of the Andes of Colombia, Ecuador, Peru and northern Bolivia, and development of the Amazonian foreland, was initiated during Late Cretaceous-Paleocene times and followed by an unloading stage during the Early-Middle Eocene period. The Middle-Late Eocene marine transgression and the increase in sedimentation rates, associated with westward migration of the depocentre, were all indicative of a renewed phase of tectonic loading of the Peruvian Western Cordillera and the Ecuadorian and Colombian Eastern Cordillera. Subsequent Oligo-Miocene increase in sedimentation rates and further migration of the depocentres towards the present-day sub-Andean zone, are all indicative for a thrust-induced uplift and loading of the Eastern Cordilleras of Peru, Bolivia and Colombia. This Oligo-Miocene loading stage maintained high subsidence rates that favoured the sedimentation of aggradational fl oodplain and coastal plain and tidally infl uenced deposits. Nevertheless, the processes that controlled the Early-Middle Miocene marine ingressions remain to be determined. Late Miocene ongoing thrust tectonic loading of the Eastern Cordillera, initial structuring of the sub-Andean zone and the onset of the main phase of Andean surface uplift induced fl exural subsidence in the foredeep depozones of the entire Amazonian foreland basin. This process also drove the Late Miocene marine transgressions that characterized the fi lled stage of the Ecuadorian, Peruvian and Bolivian Amazonian foreland basin system. Valley incisions and full relief development in the hinterland during the Late Miocene-Pliocene provided increased sediment supply and overfi lled the Amazonian foreland basin system. Finally, the fl at-slab subduction of the Nazca ridge induced Pliocene (~4 Ma) uplift of the Fitzcarrald Arch and subdivided the Amazonian foreland basin into the northern and southern Amazonian foreland basins.

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“…Tectonic, eustatic, climatic, and autocyclic processes are commonly invoked as the major factors controlling sedimentation and stacking patterns in basins (for example, Schumm, 1977;Bridge and Leeder, 1979;Miall, 1988;Flemings and Jordan, 1990;Vail and others, 1991;Schumm, 1993;Cant, 1998;Catuneanu, 2004). Active tectonism is considered to be a major factor driving recurring episodes of subsidence and uplift in basins (Bridge and Leeder, 1979;Heller and others, 1988;Flemings and Jordan, 1990;Heller and Paola, 1996).…”

Section: Discussionmentioning

confidence: 99%

“…As orogenic loading increases, subsidence rates increase in areas proximal to the orogenic belt. The basin is typically underfilled (Catuneanu, 2004), and with an increase in subsidence, fine-grained, low-energy facies with low channel densities (Heller and Paola, 1996) and reduced sandbody interconnectedness (Bridge and Leeder, 1979) are deposited in proximal areas just beyond the coarsest-grained wedges (Flemings and Jordan, 1990).…”

Section: Discussionmentioning

confidence: 99%

Depositional environments of the Prince Creek Formation along the east side of the Toolik River, Sagavanirktok Quadrangle, North Slope, Alaska

Flaig¹,

Kolk²

2015

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Retroarc foreland systems––evolution through time

Cited by 166 publications

References 36 publications

Meso-Archaean and Palaeo-Proterozoic sedimentary sequence stratigraphy of the Kaapvaal Craton

Meso-Archaean and Palaeo-Proterozoic sedimentary sequence stratigraphy of the Kaapvaal Craton

Cenozoic Sedimentary Evolution of the Amazonian Foreland Basin System

Depositional environments of the Prince Creek Formation along the east side of the Toolik River, Sagavanirktok Quadrangle, North Slope, Alaska

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