Abstract
Abstract. In polar regions, sastrugi are a direct manifestation of drifting snow and form the main surface roughness elements. In turn, sastrugi alter the generation of atmospheric turbulence and thus modify the wind field and the aeolian snow mass fluxes. Little attention has been paid to these feedback processes, mainly because of experimental difficulties. As a result, most polar atmospheric models currently ignore sastrugi over snow-covered regions. This paper aims at quantifying the potential influence of sastrugi on the local wind field and on snow erosion over a sastrugi-covered snowfield in coastal Adélie Land, East Antarctica. We focus on two erosion events during which sastrugi responses to shifts in wind direction have been interpreted from temporal variations in drag and aeolian snow mass flux measurements during austral winter 2013. Using this data set, it is shown that (i) neutral stability, 10 m drag coefficient (CDN10) values are in the range of 1.3–1.5 × 10−3 when the wind is well aligned with the sastrugi, (ii) as the wind shifts by only 20–30° away from the streamlined direction, CDN10 increases (by 30–120 %) and the aeolian snow mass flux decreases (by 30–80 %), thereby reflecting the growing contribution of the sastrugi form drag to the total surface drag and its inhibiting effect on snow erosion, (iii) the timescale of sastrugi aerodynamic adjustment can be as short as 3 h for friction velocities greater than 1 m s−1 and during strong drifting snow conditions and (iv) knowing CDN10 is not sufficient to estimate the snow erosion flux that results from drag partitioning at the surface because CDN10 includes the contribution of the sastrugi form drag.
Highlights
IntroductionSastrugi are a direct manifestation of drifting snow
In polar regions, sastrugi are a direct manifestation of drifting snow
– CDN10 values are in the range of 1.3–1.5 × 10−3 when the wind is well aligned with the sastrugi
Summary
Sastrugi are a direct manifestation of drifting snow They are generally regarded as elongated ridges of wind-packed snow 1 to 2 m in length, with a longitudinal axis parallel to the prevailing wind at the time of their formation. These erosional surface roughness features are very widespread over the Antarctic ice sheet (Kotlyakov, 1961), where they can be major determinants of surface roughness (Jackson and Carroll, 1978; Inoue, 1989; Andreas and Claffey, 1995). Schmidt (1980) reported that the cohesion of the snow surface determines the threshold speed required for snow erosion to occur. Budd et al (1966) suggested a high threshold wind speed (14 m s−1) was needed to trigger snow transport in the cold environment of Byrd station. Schmidt (1980) reported that the cohesion of the snow surface determines the threshold speed required for snow erosion to occur. Schmidt (1980) showed that the threshold wind speed increases with time since snow depo-
Sign-in/Register to view highlights & summary Sign-in/Register to access full text options 
Free) 
Talk to us
Join us for a 30 min session where you can share your feedback and ask us any queries you have
Schedule a call
