Structures developed by dissipation of dune and beach ridge deposits

Bigarella, João José

doi:10.1016/s0341-8162(75)80008-7

Cited by 34 publications

(28 citation statements)

References 6 publications

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“…Fluidization and erosion of dune lee faces and the resulting deposits have been recognized in modern settings, such as the Brazil coast (Bigarella 1975), the Nebraska Sand Hills (Sweeny and Loope 2001), the Devonian of Antarctica (Wizevich 1997) and the Cretaceous of the Nemegt basin in Mongolia (Loope et al 1998;Loope et al 1999). All of these studies have invoked extreme precipitation events as the triggering mechanism for modification of dune lee faces.…”

Section: Discussionmentioning

confidence: 99%

“…In modern and ancient eolian settings, the origin of massive sandstone bodies interbedded with eolian stratification has been the subject of increased scrutiny because of their potential as paleoenvironmental and paleoclimatic indicators (e.g., Bigarella 1975;Kocurek 1981;Hummel and Kocurek 1984;Wizevich 1997;Loope et al 1998;Loope et al 1999;Sweeney and Loope 2001). In ancient successions, bodies of massive sandstone have been reported interbedded with interdune deposits and in association with high-angle and low-angle eolian dune cross strata (e.g., Ahlbrandt and Fryberger 1981;Hunter 1981;Kocurek 1981;Hummel and Kocurek 1984;Wizevich 1997;Loope et al 1998;Loope et al 1999).…”

Section: Introductionmentioning

confidence: 99%

“…In ancient successions, bodies of massive sandstone have been reported interbedded with interdune deposits and in association with high-angle and low-angle eolian dune cross strata (e.g., Ahlbrandt and Fryberger 1981;Hunter 1981;Kocurek 1981;Hummel and Kocurek 1984;Wizevich 1997;Loope et al 1998;Loope et al 1999). Where interbedded with dune cross strata, massive sandstones have been interpreted variously as: (1) products of mass flows, generated during marine transgression (Eschner and Kocurek 1986;Kamola and Chan 1988), (2) products of fluvial incursions or fluvial interactions with the dunefield (Chakraborty and Chaudhuri 1993;Herries 1993;Wizevich 1997), or (3) degradation of dunes by extreme precipitation events (Bigarella 1975;Williams 1978, 1979;Sweeny and Loope 2001).…”

Section: Introductionmentioning

confidence: 99%

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Eolian Dune Degradation and Generation of Massive Sandstone Bodies in the Paleoproterozoic Makgabeng Formation, Waterberg Group, South Africa

Simpson¹,

Eriksson²,

Eriksson³

et al. 2002

Journal of Sedimentary Research

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Massive sandstone bodies in the 1.85 Ga Makgabeng Formation, South Africa, are located within the middle and upper part of the formation and are associated with the oldest reported deposits of barchan and barchanoid-ridge dunes. Bases of massive sandstone bodies are channelized or planar. Channel-based bodies typically overlie low-angle or up to 26؇ inclined wind-ripple strata. Channel margins vary from low angle to vertical. Rarely, massive sandstones at channel margins display vague horizontal stratification and/or contain rippedup fragments of wind-ripple strata. Planar-based massive sandstone bodies are lenticular and characteristically are interbedded with lowangle to horizontal dune toesets. These lobate massive sandstone bodies vary from 5 cm to 6 m in thickness and from 3 m to possibly over 50 m in width; some of the sandstone bodies onlap dune reactivation surfaces. Rare dewatering structures, parting lineations, and adhesion structures occur at tops of the massive sandstone bodies. Lower boundaries of massive sandstone bodies change from channelized to planarbased down the dune foresets.Massive sandstones were generated by two different mechanisms, which are inferred to have been triggered by significant precipitation events. The presence of steep margins, channeling, rip-up fragments, and dewatering features, and a lack of tractional structures, indicate that most massive sandstones were deposited from hyperconcentrated flows down the dune lee face. Flows were initially turbulent, analogous to hyperconcentrated flows, resulting in scouring of wind-ripple strata. As hyperconcentrated flows migrated onto the dune plinth, rapid deposition produced lobate massive sandstone deposits with planar bases. This sedimentation is linked to development of a hydraulic jump at the slipface-plinth intersection, which increased flow depth and reduced flow velocity. Some flows maintained their turbulence onto the dune plinth, resulting in erosion of the plinth and scouring into the underlying preserved dune deposits. Massive sandstone bodies linked to reactivation surfaces are more likely a result of partial lee-face collapse, which generated translational slides.

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Section: Discussionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Eolian Dune Degradation and Generation of Massive Sandstone Bodies in the Paleoproterozoic Makgabeng Formation, Waterberg Group, South Africa

Simpson¹,

Eriksson²,

Eriksson³

et al. 2002

Journal of Sedimentary Research

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“…Research on the dynamics of parabolic dunes has focused on several key areas including: (i) dune distribution and morphology (Landsberg, 1956;Cooper, 1958;David, 1977David, , 1981Pye, 1982;Anton and Vincent, 1986;Pye, 1993;Wolfe and David, 1997); (ii) timing of past dune activity (Wolfe et al, 1995;David et al, 1999;Wolfe et al, 2000Wolfe et al, , 2001Arbogast et al, 2002;Forman and Pierson, 2003;Havholm and Running, 2005); (iii) rates of migration (Cooper, 1958;Pye, 1982;Anthonsen et al, 1996;David et al, 1999;Craig, 2000;Tsoar and Blumberg, 2002;Bailey and Bristow, 2004;Marín et al, 2005); (iv) internal structure (Bigarella, 1975;Halsey et al, 1990); and (v) contemporary processes (Robertson-Rintoul, 1990;Arens et al, 2004). Despite this progress, the current understanding of parabolic dune morphodynamics is based solely on investigations of form and process in two dimensions (i.e., plan view or profile form).…”

Section: Introductionmentioning

confidence: 99%

Spatial and temporal patterns of aeolian sediment transport on an inland parabolic dune, Bigstick Sand Hills, Saskatchewan, Canada

et al. 2009

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“…Research on the dynamics of parabolic dunes has focused on several key topics including: (i) dune distribution and morphology (Landsberg, 1956;Cooper, 1958;David, 1977David, , 1981Pye, 1982;Anton and Vincent, 1986;Pye, 1993;Wolfe and David, 1997); (ii) timing of past dune activity (Wolfe et al, 1995;David et al, 1999;Wolfe et al, 2000Wolfe et al, , 2001Arbogast et al, 2002;Forman and Pierson, 2003;Havholm and Running, 2005); (iii) rates of migration (Cooper, 1958;Pye, 1982;Anthonsen et al, 1996;David et al, 1999;Craig, 2000;Tsoar and Blumberg, 2002;Bailey and Bristow, 2004;Marín et al, 2005); (iv) internal structure (Bigarella, 1975;Halsey et al, 1990); and (v) contemporary processes (Robertson-Rintoul, 1990;Arens et al, 2004). Despite this progress, they do represent the best-studied type of dunes, and both their morphological and dynamic parameters are well understood (e.g.…”

mentioning

confidence: 99%

Statistical Modeling of Morphological Parameters of Barchan Dunes (Case Study: Chah Jam Erg in South of Haj Ali GHoli Playa, in Central Part of Semnan Province, IRAN)

Mousavi¹,

Dorgouie²,

Vali³

et al. 2010

JGG

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A wide variety of aeolian sand dunes are found in Chah Jam erg, in central part of IRAN, best known type of them are the barchan dunes, shaped in a crescent, which occur if the wind comes steadily from the same direction throughout the year and if there is not enough sand to cover the entire surface. Barchan dunes in studied area are moving to 20 m/year toward S-SW. Their speed is dependent on wind velocity, three dimensional morphology and interaction between them. In this study, morphological parameters of barchan dunes and their annual movement rate (from 1/4/2008 to 1/4/2009) have been measured. Then using regression analysis method, type and intensity of relationship between morphological parameters and movement rate have been reexamined. These relationships follow simple and multivariable liner, power and exponential relations. Finally, we represented the models, by using them, can easily assess annual movement rate of Barchan dunes.

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Structures developed by dissipation of dune and beach ridge deposits

Cited by 34 publications

References 6 publications

Eolian Dune Degradation and Generation of Massive Sandstone Bodies in the Paleoproterozoic Makgabeng Formation, Waterberg Group, South Africa

Eolian Dune Degradation and Generation of Massive Sandstone Bodies in the Paleoproterozoic Makgabeng Formation, Waterberg Group, South Africa

Spatial and temporal patterns of aeolian sediment transport on an inland parabolic dune, Bigstick Sand Hills, Saskatchewan, Canada

Statistical Modeling of Morphological Parameters of Barchan Dunes (Case Study: Chah Jam Erg in South of Haj Ali GHoli Playa, in Central Part of Semnan Province, IRAN)

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