Migration and stratigraphic fill of an underfilled foreland basin: Middle–Late Cenomanian Belle Fourche Formation in southern Alberta, Canada

Yang, Yanchu; Miall, Andrew D.

doi:10.1016/j.sedgeo.2010.03.005

Cited by 15 publications

(9 citation statements)

References 30 publications

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“…Beaumont 1981). The gradual and systematic facies changes (both laterally and vertically) exhibited by the Morar Group and the lack of sharp influxes of coarse deposits are consistent with the genesis of the basin under a suite of conditions such that the rate of subsidence exceeded the rate of sediment flux, a pattern not uncommon in foreland settings (Tankard 1986;Varban & Plint, 2008;Yang & Miall 2010). The palaeocontinental reconstructions also indicate that the Moine basin was located relatively near to the periphery of Rodinia (Li et al 2008; see also Cawood et al 2010), so that the evolving basin may also have been affected by far-field plate boundary effects and sea-level changes, similar to those which would have affected correlative successions in East Greenland and Svalbard (Cawood et al 2010).…”

Section: Allen and Allen 2005)mentioning

confidence: 56%

“…Cretaceous Interior Seaway basins that fringed the North American Cordillera from Canadian to Mexico (Beaumont, 1981;Flemings & Jordan 1989;Cant & Stockmal 1989;Flemings & Jordan 1990;Jordan & Flemings 1991;Underschultz & Erdmer 1991;Plint et al 2001;Varban & Plint 2008;Yang & Miall 2010). There, episodic loading events are known to have driven km-scale progradational-retrogradational depositional cycles, not dissimilar to those described above for the Morar Group.…”

Section: Allen and Allen 2005)mentioning

confidence: 92%

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Sedimentology of the early Neoproterozoic Morar Group in northern Scotland: implications for basin models and tectonic setting

Bonsor

Strachan

Prave

et al. 2012

JGS

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The metasedimentary rocks of the Morar Group in northern Scotland form part of the early Neoproterozoic Moine Supergroup. The upper part of the Group is c. 2-3 km thick and contains two large km-scale facies successions: a coarsening-upwards marine-to-fluvial regression overlain by a fining-upwards fluvial-to-marine transgression. Fluvial facies make up less than a third of the total thickness; shallow-marine lithofacies comprise the remainder.Combining these new findings with previously published data indicates that the Morar Group represents, overall, a transgressive stratigraphic succession c. 6-9km thick, in which there is both an upward and eastward predominance of shallow-marine deposits, and a concomitant loss of fluvial facies. Smaller-scale (100s of m thick) transgressive-regressive cycles are superimposed on this transgressive trend. Collectively, the characteristics of the succession are consistent with deposition in a foreland basin located adjacent to the Grenville orogen, and possibly linked to the peri-Rodinian ocean. Subsidence and progressive deepening of the Morar basin may have, at least in part, been driven by loading of Grenville-orogenyemplaced thrust sheets, and aided by sediment loading. However, the relative contributions of thrust loading versus plate boundary effects and/or eustatic sea-level rise on basin evolution remain speculative.

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Section: Allen and Allen 2005)mentioning

confidence: 56%

Section: Allen and Allen 2005)mentioning

confidence: 92%

Sedimentology of the early Neoproterozoic Morar Group in northern Scotland: implications for basin models and tectonic setting

Bonsor

Strachan

Prave

et al. 2012

JGS

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“…Several models were suggested to explain the relations between thrust loading, sediment supply, and basin shape (Flemings & Jordan 1989;Jordan & Flemings 1991), basin character and depozone migration (Heller et al 1988;Catuneanu et al 1998;Yang & Miall 2010). The principal data about the alternating phases of thrusting activity (orogenic loading) and tectonic quiescence (sediment loading) are provided by the study of either the proximal foredeep or the forebulge depozones (Flemings & Jordan 1989;Jordan & Flemings 1991;Sinclair et al 1991;Crampton & Allen 1995;Plint 2000;Plint et al 2001;Yang & Miall 2010;Leszczyński & Nemec 2014). However, as thrust movement propagates further and further onto the foreland, the foreland basin structure is "continually" modified as inner parts of the basin (proximal to active margin) are incorporated into the anticlinal thrust stack, and basin depozones are shifted further onto the foreland.…”

Section: Introductionmentioning

confidence: 99%

Evolution of the passive margin of the peripheral foreland basin: an example from the Lower Miocene Carpathian Foredeep (Czech Republic)

Francírek¹,

Nehyba²

2016

Geologica Carpathica

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Abstract:The Karpatian deposits of the central part of the Carpathian Foredeep in Moravia, which are deeply buried under the Outer Western Carpathians, provide a unique opportunity to reconstruct the former evolutionary stages of this peripheral foreland basin and its paleogeography. A succession of three depositional units characterized by a distinct depositional environment, provenance, and partly also foreland basin depozone, have been identified. The first depositional unit represents a proximal forebulge depozone and consists of lagoon-estuary and barred coastline deposits. The source from the "local" crystalline basement played here an important role. The second depositional unit consists of coastline to shallow marine deposits and is interpreted as a forebulge depozone. Tidalites recognized within this unit represent the only described tide-generated deposits of the Neogene infill of the Carpathian Foredeep basin in Moravia. The source from the basin passive margin (the Bohemian Massif) has been proved. The third depositional unit is formed by offshore deposits and represents a foredeep depozone. The provenance from both passive and active basin margin (Silesian Unit of the Western Carpathian Flysch Zone) has been proved. Thus, both a stepwise migration of the foredeep basin axis and shift of basin depozones outwards/cratonwards were documented, together with forebulge retreat. The shift of the foreland basin depozones more than 50 km cratonward can be assumed. The renewed thrusting along the basin's active margin finally completely changed the basin shape and paleogeography. The upper part of the infill was deformed outside the prograding thrust front of flysch nappes and the flysch rocks together with a strip of Miocene sediments were superposed onto the inner part of the basin. The width and bathymetric gradient of the entire basin was changed/reduced and the deposition continued toward the platform. The basin evolution and changes in its geometry are interpreted as a consequence of the phases of the thrust-sheet stacking and sediment loading in combination with sealevel change.

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“…Los modelos de cuencas subalimentadas y sobrealimentadas (Yang y Miall, 2010;Yang, 2011) proveen un marco de referencia para el entendimiento de la evolución del relleno de la cuenca durante la depositación de Subgrupo Río Neuquén en su totalidad, como así también la discordancia progresiva que se observa a gran escala entre y dentro de la unidades que lo integran (Fig. 2).…”

Section: Discussionunclassified

“…Los estudios geocronológicos de los circones detríticos demuestran la presencia de edades entre 102±2 Ma y 100±8 Ma en las unidades inferiores del Grupo Neuquén (Di Giulio et al, 2012), que se interpreta como una respuesta al sistema geodinámico de la cuenca del antepaís. De acuerdo con el modelo conceptual propuesto por Yang y Miall (2010), el avance del frente de corrimiento hacia el este del cinturón plegado y corrido del Agrio (Tunik et al, 2010) ocasiona la migración del abultamiento periférico de la cuenca de antepaís, como consecuencia de la repuesta flexural de la misma.…”

Section: Estratigrafía Secuencialunclassified

Sedimentología y estratigrafía de alta resolución del subgrupo río Neuquén (Cretácico Superior) departamento confluencia, provincia de Neuquén, Argentina

Sánchez

Asurmendi

Armas

2014

Andgeo

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RESUMEN.En el sector centro-este de la Cuenca Neuquina, suroeste de Neuquén, Patagonia Argentina, el Subgrupo Río Neuquén de origen continental ha sido dividido en dos secuencias estratigráficas incompletas (SI y SII) sobre la base de discontinuidades que limitan arreglos de litofacies y elementos arquitecturales característicos. Parte de la sucesión (Formación Portezuelo-SI) se formó a partir de sistemas fluviales de baja y alta sinuosidad que drenaban hacia el noreste. La acreción lateral y oblicua es un rasgo importante de los sistemas de alta energía con carga mixta. Los depósitos de planicie de inundación dominan la estratigrafía, contribuyendo con más del 45% de los sedimentos. La Formación Plottier (SII) se acumuló a partir de un sistema de baja sinuosidad perenne con un buen desarrollo de los depósitos de planicie aluvial con eventos de inundaciones. La unidad se acumuló sobre una topografía con un gradiente general hacia el este-noreste. La arquitectura aluvial y patrones de apilamiento en el Subgrupo Río Neuquén estuvo controlada por la combinación de factores alogénicos, el más significativo fue la tectónica seguida por el clima. La sucesión del Cretácico Tardío en la cuenca de antepaís andina, depositada en la cuenca periférica, consiste de ciclos tectónicos que comprenden dos componentes: estratos depositados en una cuenca subalimentada (Formación Portezuelo, AA-SI) y sedimentación en una cuenca sobrealimentada sin un abultamiento periférico definido topográficamente (Formación Plottier, BA-SII). ABSTRACT. Sedimentology and high resolution stratigraphy of Río Neuquén Subgroup (Upper Cretaceous) department Confluence, Province of Neuquén, Argentina.The Upper Cretaceous exposid in the northeastern part of the Neuquén Basin, southeast of Neuquén, Argentina. Río Neuquén Subgroup of continental origin, has been divided into two incomplete stratigraphic sequence units (SI y SII) on the basis of lithofacies assemblages and architectural elements. Parts of the succession (Portezuelo Formation SI) formed in northeasward-draining low and high sinuosity fluvial systems. Those are analyzed in detail in terms of macroform-scale and stratigraphic-level architecture to assess fluvial styles and the evolution of non-marine depositional environments. Lateral and oblique accretion is a significant process of deposition in high-energy systems with mixed load. The overbank deposits dominate the floodplain stratigraphy; they contribute more than 45% of floodplain sediments. The Plottier Formation (SII) was accumulated from a low sinuosity perennial system with well developed deposits of alluvial plain with flood events. The unit was accumulated on topographic slopes dipping from west-southwest to east-northeast. The alluvial architecture and stacking patterns in the Río Neuquén Subgroup were controlled by a combination of allogenic factors, most significantly tectonics followed by climate. The Upper Cretaceous succession in the Andean foreland basin, deposited in a backbulge zone, consists of tectonically-driven cycles ...

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Migration and stratigraphic fill of an underfilled foreland basin: Middle–Late Cenomanian Belle Fourche Formation in southern Alberta, Canada

Cited by 15 publications

References 30 publications

Sedimentology of the early Neoproterozoic Morar Group in northern Scotland: implications for basin models and tectonic setting

Sedimentology of the early Neoproterozoic Morar Group in northern Scotland: implications for basin models and tectonic setting

Evolution of the passive margin of the peripheral foreland basin: an example from the Lower Miocene Carpathian Foredeep (Czech Republic)

Sedimentología y estratigrafía de alta resolución del subgrupo río Neuquén (Cretácico Superior) departamento confluencia, provincia de Neuquén, Argentina

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