Large scale sand saltation over hard surface: a controlled experiment in still air

doi:10.1007/s40333-021-0104-3

Journal of Arid Land

2021, Vol. 13

Issue (6): 599-611 DOI: 10.1007/s40333-021-0104-3 CSTR: 32276.14.s40333-021-0104-3

Research article

Large scale sand saltation over hard surface: a controlled experiment in still air

LIU Benli¹^,²^,^*(

), WANG Zhaoyun¹^,³, NIU Baicheng⁴, QU Jianjun¹^,²

¹Key Laboratory of Desert and Desertification, Northwest Institute of Eco-Environment and Resources, Chinese Academy of Sciences, Lanzhou 730000, China
²Research Station of Gobi Desert Ecology and Environment in Dunhuang of Gansu Province, Lanzhou 730000, China
³University of Chinese Academy of Sciences, Beijing 100049, China
⁴Qinghai Normal University, Xining 810004, China

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Abstract

Saltation is the major particle movement type in wind erosion process. Saltating sand grains can rebound up to tens of times larger in length and height over hard surface (such as gravel surface) than over loose sand surface. Gravels usually have different faces, causing distinct response of the impacting grains, but the effects of the grain and gravel-surface contact angle on grain rebound are not yet well quantified. We performed full-range controlled experiments of grain saltation using different contact angles, grain sizes and impact speeds in still air, to show that contact angle increases the height of representative saltation path but decreases particle travel length. The results were compared with outputs from the COMprehensive numerical model of SALTation (COMSALT). Large saltation height of 4.8 m and length of 9.0 m were recorded. The maximum and representative saltation height over the gravel surface were found to be about 4.9 times and 12.8 times those over the loose sandy surface, respectively. The maximum saltation length may be reduced by 58% and the representative saltation height may be increased by 77% as contact angle increases from 20° to 40°. We further showed that the collision inertia contributes 60% of the saltation length, and wind contributes to the other 40%. These quantitative findings have important implications for modeling saltation trajectory over gravel surface.

Key words： sand saltation trajectory gravel surface contact angle full-scale experiment

Received: 14 March 2021 Published: 10 June 2021

Corresponding Authors:

About author: LIU Benli (E-mail: liubenli@lzb.ac.cn)

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Cite this article:

LIU Benli, WANG Zhaoyun, NIU Baicheng, QU Jianjun. Large scale sand saltation over hard surface: a controlled experiment in still air. Journal of Arid Land, 2021, 13(6): 599-611.

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http://jal.xjegi.com/10.1007/s40333-021-0104-3 OR http://jal.xjegi.com/Y2021/V13/I6/599

Fig. 1 Evidence of large scale saltation over gravel surface. (a), serious sand abrasion of a wood pole on windward side from about 0.1 m to more than 1.5 m in a Gobi area of Xinjiang, but the bottom part below 0.1 m is less damaged; (b), abrasion of a concrete bridge pier (indicated by the ellipse) shows the strongest abrasion at about 0.8 m high; (c), sand deposited behind a 3.3 m high wall as wind breaker at a section of the Lanzhou-Xinjiang high-speed railway; and (d), grain-size distribution of five samples from the site shown in (c). At the three sites of (a)-(c), wind is almost unidirectional, with sand blowing toward the abrasion side in (a) and (b) but another side of the wall in (c).

Fig. 2 Equipments used in the experiments. (a), a sketch of the test equipment with the power section, control panel, contact slate with its contact angle (θ), a horizontal nozzle to simulate an impact angle (β), the liftoff angle (α) of rebound particles, and the horizontal and vertical sand-catch bins (the inset shows the relationships ofθ, α and βin details); (b), horizontal bins to collect sands on the floor; and (c), removing of vertical bins; (d), tested relationship between used pressure and air speed, in which v is impact speed and p is air pressure; (e), distribution of counted gravel inclination angles.

Fig. 3 Concentration contour maps of the saltation space for fine sand. Each column shows different impact speed (v) with the same contact angle θ, and each row shows the effect of θ under the same impact speed. Large light gray areas in each penal indicate low possibility to encounter particles, and most of the particles concentrate at a small range (the representative trajectory). Log scale is used to show the changes of region with low concentrations. Some isolated light patches exist, because zero concentration was measured below or before the patches.

Fig. 4 Concentration contour maps of the saltation space for medium sand

Fig. 5 Concentration contour maps of the saltation space for coarse sand

Fig. 6 Profiles of maximum concentration (H_c) and maximum position (H_m). Each column shows different θ, and each row shows different particle sizes. H_m is apparently higher than H_c, meaning that particles may rise to a much higher location.

Fig. 7 Characteristic trajectory values for three grain sizes (one column for each size) under different impact speeds and contact angles. L_m, maximum saltation length.

Table 1 Linear regression coefficients for L_m, H_c and H_m with impact speed v at different particle size and contact angle

Fig. 8 Relationship between saltation length/height (L_m/H_c and L_m/H_m) and liftoff angle (α) of the test results in still air. Unfilled symbols are those adjusted by 1.7 times to match blown sand results in wind tunnel experiments by Ling and Wu (1980).

Fig. 9 Comparison between the test and COMSALT-simulated L_m (a), H_m (b) and H_c (c) in still air for three particle size groups. The test is found to be conservative in reflecting saltation length (a), but clearly shows that current saltation model for flat surface conditions underestimate the saltation height over hard contact surface like the Gobi. The differences can be 4.9 times forH_m and 12.8 times for H_c.


[1]	Ammi M, Oger L, Beladjine D, et al. 2009. Three-dimensional analysis of the collision process of a bead on a granular packing. Physical Review, E79:021305, doi: 10.1103/PhysRevE.79.021305. doi: 10.1103/PhysRevE.79.021305

[2]	Ayoub F, Avouac J P, Newman C E, et al. 2014. Threshold for sand mobility on Mars calibrated from seasonal variations of sand flux. Nature Communications, 5(1):5096, doi: 10.1038/ncomms6096. doi: 10.1038/ncomms6096

[3]	Bagnold R A. 1941. The Physics of Blown Sand and Desert Dunes. London: Chapman & Hall, 72.

[4]	Bagnold R A. 1973. The nature of saltation and of 'bed-load' transport in water. Proceedings of the Royal Society of London. Mathematical and Physical Sciences, 332:473-504.

[5]	Burr D M, Bridges N T, Marshall J R, et al. 2015. Higher-than-predicted saltation threshold wind speeds on Titan. Nature, 517:60-63. doi: 10.1038/nature14088

[6]	Cheng J, Lei J, Li S, et al. 2016. Disturbance of the inclined inserting-type sand fence to wind-sand flow fields and its sand control characteristics. Aeolian Research, 21:139-150. doi: 10.1016/j.aeolia.2016.04.008

[7]	Dong Z, Liu X P, Wang X M. 2002a. Aerodynamic roughness of gravel surfaces. Geomorphology, 43(1-2):17-31. doi: 10.1016/S0169-555X(01)00097-6

[8]	Dong Z, Wang H T, Liu X P, et al. 2002b. Velocity profile of a sand cloud blowing over a gravel surface. Geomorphology, 45(3-4):277-289. doi: 10.1016/S0169-555X(01)00159-3

[9]	Dong Z, Qian G Q. 2007. Characterizing the height profile of the flux of wind-eroded sediment. Environmental Geology, 51:835-845. doi: 10.1007/s00254-006-0363-5

[10]	Hagen L J, van Pelt S, Sharratt B. 2010. Estimating the saltation and suspension components from field wind erosion. Aeolian Research, 1(3-4):147-153. doi: 10.1016/j.aeolia.2009.08.002

[11]	Ho T D, Valance A, Dupont P, et al. 2011. Scaling laws in aeolian sand transport. Physical Review Letters, 106(9):094501, doi: 10.1103/PhysRevLett.106.094501. doi: 10.1103/PhysRevLett.106.094501

[12]	Ho T D, Valance A, Dupont P, et al. 2014. Aeolian sand transport: Length and height distributions of saltation trajectories. Aeolian Research, 12:65-74. doi: 10.1016/j.aeolia.2013.11.004

[13]	Jiang C, Dong Z, Wang X. 2017. An improved particle tracking velocimetry (PTV) technique to evaluate the velocity field of saltating particles. Journal of Arid Land, 9(5):727-742. doi: 10.1007/s40333-017-0030-6

[14]	Kok J F, Renno N O. 2009. A comprehensive numerical model of steady state saltation (COMSALT). Journal of Geophysical Research-Atmospheres, 114(17), doi: 10.1029/2009jd011702. doi: 10.1029/2009jd011702

[15]	Lämmel M, Kroy K. 2017. Analytical mesoscale modeling of aeolian sand transport. Physical Review, E96:052906, doi: 10.1103/PhysRevE.96.052906. doi: 10.1103/PhysRevE.96.052906

[16]	Li S, Li C, Yao D, et al. 2020. Wind tunnel experiments for dynamic modeling and analysis of motion trajectories of wind-blown sands. The European Physical Journal, E43:22, doi: 10.1140/epje/i2020-11945-0. doi: 10.1140/epje/i2020-11945-0

[17]	Ling Y, Wu Z. 1980. Experimention on the dynamic photography of the movement of sand-driving wind. Acta Geographica Sinica, 35:174-181. (in Chinese)

[18]	Lorenz R D, Zimbelman J R. 2014. Mechanics of sand transport. In: Lorenz R D, Zimbelman J R. Dune Worlds How Windblown Sand Shapes Planetary Landscapes. Berlin: Springer, 39-54.

[19]	Pähtz T, Omeradžić A, Carneiro M V, et al. 2015. Discrete Element Method simulations of the saturation of aeolian sand transport. Physics, 42(6):2063-2070.

[20]	Reichardt H. 1941. About a new theory of free turbulence. Journal of Applied Mathematics & Mechanics, 21:257-264. (in German)

[21]	Shao Y, Raupach M R, Findlater P A. 1993. Effect of saltation bombardment on the entrainment of dust by wind. Journal of Geophysical Research: Atmospheres, 98(7):12719-12726. doi: 10.1029/93JD00396

[22]	Tan L, An Z, Zhang K, et al. 2020. Intermittent aeolian saltation over a gobi surface: threshold, saltation layer height, and high-frequency variability. Journal of Geophysical Research: Earth Surface, 125(1):e2019JF005329, doi: 10.1029/2019jf005329. doi: 10.1029/2019jf005329

[23]	Williams S H, Leer J A. 1995. Aeolian saltation transport rate: an example of the effect of sediment supply. Journal of Arid Environments, 30(2):153-160. doi: 10.1016/S0140-1963(05)80066-7

[24]	Yin Y. 1989. Study on sand drift in strong wind region in gravel desert. Journal of Desert Research, 9:27-36. (in Chinese)

[25]	Zhang K C, Qu J J, Zu R P, et al. 2008. Characteristics of wind-blown sand on Gobi/mobile sand surface. Environmental Geology, 54:411-416. doi: 10.1007/s00254-007-0827-2

[26]	Zheng X, He L, Wu J. 2004. Vertical profiles of mass flux for windblown sand movement at steady state. Journal of Geophysical Research: Solid Earth, 109(1), doi: 10.1029/2003jb002656. doi: 10.1029/2003jb002656

[27]	Zou X, Hao Q, Zhang C, et al. 1999. Parameter analysis on the saltation trajectory of wind blown sand. Chinese Science Bulletin, 44:1084-1088. (in Chinese)

[28]	Zou X, Cheng H, Zhang C, et al. 2007. Effects of the Magnus and Saffman forces on the saltation trajectories of sand grain. Geomorphology, 90(1-2):11-22. doi: 10.1016/j.geomorph.2007.01.006

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