Unsteady saltation on Mars

Ping, Wang; Zheng, Xiaojing

doi:10.1016/j.icarus.2015.07.012

Cited by 15 publications

(12 citation statements)

References 63 publications

(95 reference statements)

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“…The findings from collision experiments with static beds are often applied to model fluvial bedload (Berzi et al, ; Pähtz, Liu, et al, ) and aeolian saltation transport (Andreotti, ; Berzi et al, , ; Bo et al, ; Claudin and Andreotti, ; Creyssels et al, ; Huang et al, ; Jenkins et al, ; Jenkins and Valance, , ; Kok, ; Kok and Renno, ; Lämmel et al, ; Lämmel and Kroy, ; Pähtz et al, ; Pähtz, Liu, et al, ; Wang and Zheng, , ). However, if the time between successive particle‐bed impacts is too short for a bed particle to fully recover from each impact, it can accumulate more and more kinetic energy with each impact.…”

Section: The Role Of Particle Inertia In Nonsuspended Sediment Transportmentioning

confidence: 99%

The Physics of Sediment Transport Initiation, Cessation, and Entrainment Across Aeolian and Fluvial Environments

Pähtz

Clark

Valyrakis

et al. 2020

Reviews of Geophysics

121

149

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Predicting the morphodynamics of sedimentary landscapes due to fluvial and aeolian flows requires answering the following questions: Is the flow strong enough to initiate sediment transport, is the flow strong enough to sustain sediment transport once initiated, and how much sediment is transported by the flow in the saturated state (i.e., what is the transport capacity)? In the geomorphological and related literature, the widespread consensus has been that the initiation, cessation, and capacity of fluvial transport, and the initiation of aeolian transport, are controlled by fluid entrainment of bed sediment caused by flow forces overcoming local resisting forces, whereas aeolian transport cessation and capacity are controlled by impact entrainment caused by the impacts of transported particles with the bed. Here the physics of sediment transport initiation, cessation, and capacity is reviewed with emphasis on recent consensus‐challenging developments in sediment transport experiments, two‐phase flow modeling, and the incorporation of granular physics' concepts. Highlighted are the similarities between dense granular flows and sediment transport, such as a superslow granular motion known as creeping (which occurs for arbitrarily weak driving flows) and system‐spanning force networks that resist bed sediment entrainment; the roles of the magnitude and duration of turbulent fluctuation events in fluid entrainment; the traditionally overlooked role of particle‐bed impacts in triggering entrainment events in fluvial transport; and the common physical underpinning of transport thresholds across aeolian and fluvial environments. This sheds a new light on the well‐known Shields diagram, where measurements of fluid entrainment thresholds could actually correspond to entrainment‐independent cessation thresholds.

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Section: The Role Of Particle Inertia In Nonsuspended Sediment Transportmentioning

confidence: 99%

The Physics of Sediment Transport Initiation, Cessation, and Entrainment Across Aeolian and Fluvial Environments

Pähtz

Clark

Valyrakis

et al. 2020

Reviews of Geophysics

121

149

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“…Specifically, light sand grains majorly present wall-parallel translation with minor vertical sedimentation, while the descending heavy sand grains towards the wall are compensated by the quasi-constant sand-grain flux from higher layer. On the other hand, the spatial developing nature of the sand-grain motion in the near-wall region might be associated with the particle saltation process due to the combined effect of inter-particle collision, particle-wall interaction and induction of inner-layer turbulent cycle (Zheng 2009;Wang and Zheng 2015). This leads to a continuous reduction of the sand-grain kinetic energy (see figure 7a) and a persistent enhancement of the particle accumulation (see figure 7b) in the downstream.…”

Section: Partition Of the Sand Motionmentioning

confidence: 99%

Sand-turbulence interaction in a high-Reynolds-number turbulent boundary layer under net sedimentation conditions

Zhu

Pan

Wang

et al. 2019

International Journal of Multiphase Flow

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“…If V is assumed to increase linearly with u ∗ then

Q \propto u_{*} τ_{normalex}

, while if V is constant with u ∗ then

Q \propto τ_{normalex}

. Previous work has assumed a linear increase of V with u ∗ (e.g., Almeida et al, ; Armstrong & Leovy, ; Wang & Zheng, ; White, ), while recent work suggests that the relation

Q \propto τ_{normalex}

should be used (Sullivan & Kok, ).…”

Section: Model Descriptionmentioning

confidence: 99%

Crater Mound Formation by Wind Erosion on Mars

2018

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Most of Mars' ancient sedimentary rocks by volume are in wind‐eroded sedimentary mounds within impact craters and canyons, but the connections between mound form and wind erosion are unclear. We perform mesoscale simulations of different crater and mound morphologies to understand the formation of sedimentary mounds. As crater depth increases, slope winds produce increased erosion near the base of the crater wall, forming mounds. Peak erosion rates occur when the crater depth is ∼2 km. Mound evolution depends on the size of the host crater. In smaller craters mounds preferentially erode at the top, becoming more squat, while in larger craters mounds become steeper sided. This agrees with observations where smaller craters tend to have proportionally shorter mounds and larger craters have mounds encircled by moats. If a large‐scale sedimentary layer blankets a crater, then as the layer recedes across the crater it will erode more toward the edges of the crater, resulting in a crescent‐shaped moat. When a 160 km diameter mound‐hosting crater is subject to a prevailing wind, the surface wind stress is stronger on the leeward side than on the windward side. This results in the center of the mound appearing to “march upwind” over time and forming a “bat‐wing” shape, as is observed for Mount Sharp in Gale crater.

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Unsteady saltation on Mars

Cited by 15 publications

References 63 publications

The Physics of Sediment Transport Initiation, Cessation, and Entrainment Across Aeolian and Fluvial Environments

The Physics of Sediment Transport Initiation, Cessation, and Entrainment Across Aeolian and Fluvial Environments

Sand-turbulence interaction in a high-Reynolds-number turbulent boundary layer under net sedimentation conditions

Crater Mound Formation by Wind Erosion on Mars

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