Ancient river systems in the Himalayan foredeep, Chinji Village area, northern Pakistan

Willis, Brian J.

doi:10.1016/0037-0738(93)90151-t

Cited by 142 publications

(125 citation statements)

References 53 publications

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“…† Channels Rivers are fundamentally channelized (e.g. Campbell 1976;Miall 1992;Best & Bristow 1993;Marzo & Puigdefábregas 1993;Willis 1993a;Collinson 1996). Alluvial fans are constructed primarily by sheet-flooding or sediment gravity flows, and composed of relatively tabular sedimentary bodies (Blair & McPherson 1994).…”

Section: Eagle Mountain Formationmentioning

confidence: 99%

Observations from the Basin and Range Province (western United States) pertinent to the interpretation of regional detachment faults

Christie‐Blick

Anders

Wills

et al. 2007

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This paper summarizes the results of completed and ongoing research in three areas of the Basin and Range Province of the western United States that casts doubt on the interpretation of specific regional detachment faults and the large extensional strains with which such faults are commonly associated. Given that these examples were influential in the development of ideas about low-angle normal faults, and particularly in making the case for frictional slip at dips of appreciably less than the 308 lock-up angle for m 0.6 (where m is the coefficient of friction), we advocate a critical re-examination of interpreted detachments elsewhere in the Basin and Range Province and in other extensional and passive margin settings.The Sevier Desert 'detachment' of west-central Utah is reinterpreted as a Palaeogene unconformity that has been traced to depth west of the northern Sevier Desert basin along an unrelated seismic reflection (most probably a splay of the Cretaceous-age Pavant thrust). The absence of evidence in well cuttings and cores for either brittle deformation (above) or ductile deformation (below) is inconsistent with the existence of a fault with as much as 40 km of displacement. The Pavant thrust and the structurally higher Canyon Range thrust are erosionally truncated at the western margin of the southern Sevier Desert basin, and are not offset by the 'detachment' in the manner assumed by those inferring large extension across the basin.The Mormon Peak detachment of SE Nevada is reinterpreted as a series of slide blocks on the basis of detachment characteristics and spatially variable kinematic indicators that are more closely aligned with the modern dip direction than the inferred regional extension direction. A particularly distinctive feature of the detachment is a basal layer of up to several tens of centimetres of polymictic conglomerate that was demonstrably involved in the deformation, with clastic dykes of the same material extending for several metres into overlying rocks in a manner remarkably similar to that observed at rapidly emplaced slide blocks. The Castle Cliff detachment in the nearby Beaver Dam Mountains of SW Utah is similarly regarded as a surficial feature, as originally interpreted, and consistent with its conspicuous absence in seismic reflection profiles from the adjacent sedimentary basin.The middle Miocene Eagle Mountain Formation of eastern California, interpreted on the basis of facies evidence and distinctive clast provenance to have been moved tectonically more than 80 km ESE from a location close to the Jurassic-age Hunter Mountain batholith of the Cottonwood Mountains, is reinterpreted as having accumulated in a fluvial-lacustrine rather than alluvial fanlacustrine setting, with no bearing on either the amount or direction of tectonic transport. The conglomeratic rocks upon which the provenance argument was based are pervasively channelized, with erosional relief of less than 1 m to as much as 15 m, fining-upwards successions at the same scale and abundant trough ...

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Section: Eagle Mountain Formationmentioning

confidence: 99%

Observations from the Basin and Range Province (western United States) pertinent to the interpretation of regional detachment faults

Christie‐Blick

Anders

Wills

et al. 2007

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“…Downstream migration of dunes is indicated by vertical stacking of truncating trough crossbeds. In contrast, lateral accretion surfaces display small upwardfining cycles and abundant reactivation surfaces that are consistent with gradual channel abandonment (Willis, 1993). The planar-bedded and planar crossbedded structures represent upper flow regime sands (faciès Sh) and linguoid or transverse bars (faciès Sp), respectively.…”

Section: Conglomerate Facies Association-i (Cfa-i)mentioning

confidence: 94%

“…Bedload transport dominated during the depostion of the QSFA, as indicated by the ubiquitous presence of cosets of truncating trough crossbeds. The dominance of these structures can be attributed to the in-channel migration of sinuous-crested megaripples (Mueller and others, 1994), downstream migration of lower point bars (Eriksson, 1978), or a combination of the two where sand bars were covered by sinuous-crested dunes in the deeper parts of channels (Willis, 1993). Large channels are composed of composite bedforms common to fluvial sequences.…”

Section: Quartz-rich Sandstone Facies Association (Qsfa)mentioning

confidence: 99%

“…Large channels are composed of composite bedforms common to fluvial sequences. Reactivation surfaces suggest lateral sandbar migration (R0e and Hermansen, 1993;Willis, 1993) caused by a change in flow direction or periodic flow fluctuations (Rainbird, 1992). Vertical aggradation of truncating cosets of medium-to large-scale trough crossbeds resulted from megaripple progradation along channel bottoms during relatively high and constant flow stages.…”

Section: Quartz-rich Sandstone Facies Association (Qsfa)mentioning

confidence: 99%

“…The absence of fining-upward cycles common to fluvial processes (Walker and Cant, 1984;Willis, 1993) (Eriksson and others, 1994), the Lalla Rookh Basin (Eriksson and others, 1994), and the Panorama Formation (DiMarco and Lowe, 1989) of the Pilbara Block. Clast population analyses in conglomerate beds have been employed in the strike-slip basins others, 1991, 1994) and dissected arc basins (Mueller and Dimroth, 1987) of the Archean Abitibi greenstone belt.…”

Section: Quartz-rich Sandstone Facies Association (Qsfa)mentioning

confidence: 99%

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Implications of an archean strike-slip basin :

Corcoran¹

1996

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RESUMELa formation de Beaulieu Rapids est une séquence sédimentaire de 0,2 à 1 km d'épaisseur située au centre-sud de la Province structurale de l'Esclave. La formation représente un bassin en décrochement archéen qui s'est développé le long d'une faille majeure de direction NS. Des petits plutons de porphyres quartzo-feldspathiques à hornblende sont localisés le long de la zone de faille. Des datations U-Pb sur zircons donnent un âge approximatif de 2.6 Ga pour ces plutons. La présence de fragments de porphyres dans les conglomérats indique que la formation de Beaulieu Rapids doit conséquemment être plus jeune que cet âge. La marge ouest du basin est caractérisée par une discordance que sépare la ceinture volcanique de Rivière Beaulieu de la succession sédimentaire. Des failles NE tardives sont présentes sur les bordures nord et sud du bassin.Structuralement, la formation est caractérisée par une foliation penetrative NNE et par des plis en échelons dont l'orientation dominante est aussi NNE. Les plis se présentent sous la forme d'une alternance d'anticlinaux et de synclinaux localisés majoritairement dans la partie nord du bassin. Dans ce secteur, la direction de la polarité change rapidement alors que dans la partie sud du bassin les lits sont de direction nord avec une polarité généralement vers l'est. Quelques lits sont renversés mais les lits normaux sont plus communs.Les roches sédimentaires du bassin de Beaulieu Rapids montrent deux cycles positifs qui indiquent un contrôle tectonique sur la sédimentation. Le premier cycle est représenté par l'association de faciès du conglomérat I (CFA-I: Conglomerate faciès association I) et le faciès de siltstone-grès sus-jacent (SSFA: Siltstone-sandstone faciès association). L'association de faciès du conglomérat II (CFA-II: Conglomerate faciès association H) et l'association de faciès de grès riche en quartz (QSFA: Quartz-rich sandstone faciès association) qui se trouve juste au-dessus forment ensemble le second cycle de dépôt. Le CFA-I regroupe un conglomérat à cailloux et galets massif à stratifié et un conglomérat à support de matrice. Le premier est caractérisé par des conglomérats massifs à faiblement stratifiés (faciès Gm) et à lits entrecroisés en forme de fosse (Gt) à support de fragments, des conglomérats massifs à support de matrice (Gms), une unité mineure de grès à stratifications horizontales (faciès Sh) et entrecroisées (faciès St, Sp) et une argilite (FI). Localement, les galets deviennent imbriqués et montrent une composante d'écoulement NE prononcée. Le conglomérat massif à stratifié à cailloux et galets se compose des faciès Gm, Gt, Gp, St, Sh et Sp. Le CFA-I a été déposé par coulées de débris (Gms), courants de traction (Gm-Gt-StSp-Sh) et coulées en feuillets respectivement sur les portions proximale, médiale et distale du cône alluvionnaire. L'association de faciès du siltstone-grès contient une sous-unité dominée par des grès et caractérisée par les faciès Sp, St, Sh et FI qui se sont formés en raison de la migration des dunes et dépôts de levée...

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Emergent facies patterns within fluvial channel belts

Willis

Sech

2018

Fluvial Meanders and Their Sedimentary Products in the Rock Record

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Ancient river systems in the Himalayan foredeep, Chinji Village area, northern Pakistan

Cited by 142 publications

References 53 publications

Observations from the Basin and Range Province (western United States) pertinent to the interpretation of regional detachment faults

Observations from the Basin and Range Province (western United States) pertinent to the interpretation of regional detachment faults

Implications of an archean strike-slip basin :

Emergent facies patterns within fluvial channel belts

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