Sublimation of blowing snow is an important parameter not only for
the study of polar ice sheets and glaciers, but also for maintaining the
ecology of arid and semi-arid lands. However, sublimation of near-surface
blowing snow has often been ignored in previous studies. To study
sublimation of near-surface blowing snow, we established a sublimation of
blowing snow model containing both a vertical moisture diffusion equation and a
heat balance equation. The results showed that although sublimation of
near-surface blowing snow was strongly reduced by a negative feedback effect,
due to vertical moisture diffusion, the relative humidity near the surface
does not reach 100 %. Therefore, the sublimation of near-surface blowing
snow does not stop. In addition, the sublimation rate near the surface is 3–4
orders of magnitude higher than that at 10 m above the surface and the mass
of snow sublimation near the surface accounts for more than half of the
total snow sublimation when the friction wind velocity is less than about
0.55 m s
Blowing snow is the main source of polar ice sheets and mountain glaciers in
snowy areas at high latitudes in the Northern Hemisphere (such as the north of
Canada, Greenland, etc.), and these have profound influence on the global
hydrologic cycle, climate change and the ecological system. Extensive studies
have shown that sublimation of blowing snow is an important method affecting snow distribution, especially in the polar ice sheets, highland
mountains and high-latitude areas in the Northern Hemisphere. The mass of sublimated blowing snow has been found to be equal to 18.3 % of annual
precipitation in coastal Antarctica (Pomeroy and Jone, 1995), 22 % of
winter precipitation in Arctic Alaska (Liston and Sturm, 2004),
17–19 % of annual precipitation in the Rocky Mountains, Canada (MacDonald
et al., 2010), and 24 % of annual precipitation in the western Chinese
mountains (Zhou et al., 2014). In addition, the fluxes of sublimated snow
during blowing snow returned 10
Some scientists (Pomeroy and Essery, 1999; Cullen et al., 2007; Marks et al., 2008; Reba et al., 2012) used eddy covariance to directly measure sublimation of blowing snow. However, since this method can only obtain information from a few points, it is difficult to use it to predict overall sublimation in snowy areas (Pomeroy and Essery, 1999; Cullen et al., 2007; Marks et al., 2008; Reba et al., 2012). Therefore, the study of sublimation of snow using a numerical model is desirable.
The sublimation of blowing snow particles is normally accompanied by heat absorption and water vapour production, which leads to decreased ambient air temperature and increased humidity. The latter will in turn inhibit snow sublimation, and the former will decrease the saturated vapour pressure in the air, and subsequently inhibit the snow sublimation. Many researchers (Déry et al., 1998; Bintanja, 2001; Mann et al., 2000) believed that the sublimation of snow particles near the surface would be significant at the early stage of a drifting snow process. However, the high concentration of snow particles near the surface would result in a rapid air temperature decrease and humidity increase. Therefore, the humidity near surface would quickly reach saturation, leading to sublimation ceasing in the layer with saturated humidity. As a result, the sublimation of snow particles near surface would be negligible in fully developed drifting snow (Déry et al., 1998; Bintanja, 2001; Mann et al., 2000). However, some researchers (Schmidt, 1982; Groot Zwaadtink et al., 2011) found that humidity near the surface did not reach saturation in drifting snow in the field or in wind tunnel experiments and believed that this was caused by water transport (convection and diffusion). Déry and Yau (1999) fixed the relative humidity at 95 % instead of 100 % at the surface when simulating blowing snow sublimation and found that the time-integrated values of sublimation increased by 14 % at 95 % relative humidity compared with that at 100 % relative humidity. So they believed that the humidity near the surface is very important for the simulation of blowing snow sublimation. Huang et al. (2016) calculated the snow sublimation in the saltation layer by taking into consideration the effect of horizontal moisture convection on the non-homogeneous snow cover. Their results showed that sublimation of blowing snow in the saltation layer could not be neglected in the presence of horizontal moisture convection. But they did not discuss the sublimation near surface in areas such as polar ice sheets, snow-covered grassland, etc., where the snow cover is very large and the water convection is very weak. Therefore, studies on snow sublimation in these regions are of great interest for the understanding of global hydrological systems and ecosystems.
In previous blowing snow sublimation models, a diffusion equation was often used to describe the movement of snow particles. Although the equation is good at describing the movement of small particles well, it is less good at describing the movement of large snow particles, which are mainly distributed in the near-surface area (Déry et al., 1998; Xiao et al., 2000; Vionnet et al. 2014). Huang et al. (2016) used the Lagrangian particle tracing method to describe the movement of near-surface snow particles, and for the first time calculated the sublimation of saltating particles in the near-surface region with non-uniform snow cover. But this model did not take into consideration the turbulent suspension of snow particles. Furthermore, none of the above existing models took into consideration the effects of vertical moisture diffusion on the sublimation.
In this study, a drifting snow model was first established to describe the movement of snow particles of both saltating snow particles near surface and suspended snow particles in the higher region. Then, a sublimation model of blowing snow was built in combination with the drifting snow model, a vertical moisture diffusion equation and a heat balance equation. Next, sublimation of blowing snow at three different wind speeds was calculated and the temporal evolution and vertical profiles of temperature, relative humidity, mass concentration of snow particles and snow sublimation rate were analysed in detail. Finally, the proportions of the sublimation mass of snow particles near surface to the total sublimation mass were also given.
The horizontal wind field satisfies the Navier–Stokes equation at the
atmospheric boundary layer (Nemoto and Nishimura, 2004):
The snow particles jumping from the bed are divided into saltating and suspended particles when calculating snow particle movement. These two types of particles are distinguished based on the particle size and flow field conditions. Then the saltating particles are calculated by a Lagrange particle tracing method, and the suspended particles are calculated by diffusion equation.
The judging criteria of saltating and suspended particles are as follows
(Scott, 1995):
The motion equations of the saltating particles are as follows (Huang et al.,
2011):
The splash function fitted by Sugiura and Maeno (2000) according to the
observations of the low-temperature wind tunnel experiment was chosen:
The movement of suspended particles is described by the following vertical
diffusion equation according to horizontal uniformity condition (Déry
and Yau, 1999):
The aerodynamic entrainment equation of Shao and Li (1999) is chosen:
The sublimation formula is as follows (Thorpe and Mason, 1966):
The air heat and humidity equations are as follows (Déry and Yau, 1999;
Bintanja, 2000):
The initial potential temperature
The initial relative humidity profile is
The conversion relationship of relative humidity and specific humidity is
The calculation area is set to 1 m in length, 10 m in height and 0.01 m in
width. The time step is 10
The size distribution of snow particles used in this paper fits the results of Schmidt's (1982) field observations (Fig. 1).
Particle size distribution used in this paper, which fits the results of Schmidt's (1982) field observations.
The calculation process of our model is as follows.
We set a logarithmic wind field as the initial wind field, and give the
first take-off particle a random particle size
All the snow particles in the air are divided into saltating particles and suspended particles according to Eqs. (2) and (3). The movement of saltating particles is calculated according to Eqs. (4)–(7) and the movement of suspended particles is calculated with Eqs. (11) and (12).
If the snow particles fall on the bed, they will rebound and eject other particles which are on the bed. This process is calculated with Eqs. (8) and (9).
If the bed shear stress is greater than the threshold value, particles are
entrained from their random positions on the snow surface at vertical speed
The reaction force of the snow particles on the flow field is calculated by Eqs. (4) and (5) due to Newton's third law, and then the new flow field is calculated by Eq. (1).
The air temperature and humidity are calculated by Eqs. (16)–(19).
The sublimation of snow particles is calculated by Eqs. (14) and (15).
Steps (2)–(7) are recycled until the end of the simulation.
In order to verify the judging criteria in Eq. (2), we divided the particles
into sets varied by 10
Comparison of
As shown in Table 1, particles with diameter larger than the threshold diameter do not enter into air according to the vertical diffusion, indicating that these particles cannot be described by the diffusion equation. Thus, the judging criteria in Eq. (2) are reliable.
Comparison of mass concentration for this paper and field
observation
In order to verify the reliability of the blowing snow model in this paper, we compared our mass concentration results with those of the field observations (Fig. 2). The red dots in Fig. 2 show the field observation results from near Saskatoon, Canada on 26 January 1987 (Pomeroy and Male, 1992) and the black line in Fig. 2 shows our numerical simulation results using the same conditions as in the above field observation results. It is clear from Fig. 2 that our simulation results are basically consistent with those observed in the field, demonstrating the reliability of our simulations. It can be seen from Fig. 2 that there is some discontinuity in our results at a height of about 0.1 m, which is approximately equal to the maximum height of the saltating particles (Fig. 10a), for the presence of snow particles near the height of 0.1 m is rare. Therefore, the randomness of snow particles' number and their sizes at 0.1 m is relatively large, which leads to the discontinuity of snow mass concentration. This problem is more serious when the wind speed is low, for the lower the wind speed is, the fewer the number of snow particles in the air (See Fig. 2a). The situation is much improved when the wind speed is higher (see Fig. 2c).
Comparison of sublimation rate obtained this paper and by Schmidt
(1982)
We also verify the reliability of our simulation by comparing our sublimation results with those of the field observations (Fig. 3). The red lines in Fig. 3 are the observation results of Schmidt (1982) in Wyoming, USA, in 1982. The black line represents the simulated results obtained at the same environmental conditions as those of Schmidt. It can be seen that the total sublimation rates calculated using our model (black line) are approximately the same as Schmidt's results, and the sublimation rate at 0.01 m is 2 orders of magnitude larger than that at 0.1 m. These results demonstrate that our results are reliable too.
Comparison of sublimation rate for this paper and four blowing
snow models (Xiao et al., 2000). The friction velocity is set to 0.89 m s
We further compared our results with corresponding results of other models
under the same conditions. The black line in Fig. 4 represents the result of
the sublimation rate of suspended particles calculated by our model
(
Temporal evolution of mass of
Figure 5 is the temporal evolution of the mass of saltating particles and suspended particles for various friction velocities. It is shown that the masses of saltating and suspended particles increase with time, and eventually reach a steady state. The mass of saltating particles is much higher than that of suspended particles at the steady state. The time for saltating particles to reach steady state is about 2 s, and it is about 300 s for suspended particles. It can be seen that there are some fluctuations at 2–10 s. This is due to the randomness of particle movement. This also occurred in other models using a Lagrangian particle tracing method (McEwan and Willetts, 1991; Nemoto and Nishinura, 2004).
Vertical profiles of temperature and relative humidity.
Figure 6 shows the changes of temperature and humidity with height at initial state and at 1500 s. It is shown that air temperature and relative humidity are changed by sublimation of blowing snow particles, and the amplitude of these changes increases with the friction velocity. Greater wind velocity will lead to more snow particles in the air, undergoing sublimation, and subsequently more dramatic changes in air temperature and relative humidity.
Temporal evolution of temperature for various heights.
Temporal evolution of relative humidity for various heights.
Figures 7 and 8 show the temporal evolution of temperature and relative humidity at various heights. It is clear from in Figs. 7 and 8 that the amplitude changes of temperature and relative humidity decrease with height increasing and sublimation becomes weaker with increasing height while the relative humidity becomes a constant of about 2 s at 0.01 m and about 300 s at 10 m, consistent with the corresponding values for suspended snow particles. This is because the main portion of snow particles near the surface comprises saltating particles, while that in the upper air is mainly made up of suspended particles (Fig. 10).
Figure 8 also shows that the relative humidity near the surface with three friction velocities does not reach saturation when the blowing snow particles saturate, indicating that the snow sublimation does not stop. Moreover, the vertical diffusion of water vapour can effectively reduce the negative feedback effect.
Temporal evolution of saltation and suspension sublimation rates:
It can be seen from Fig. 9a that the sublimation rate of saltating particles shows a trend of first increasing then decreasing with time. Its peaks at 2 s and gradually decreases and reaches a steady state at about 300 s. The negative feedback effect on saltating particles is very obvious and the time to reach a steady state is about 300 s. The mass of saltating particles increases with time during the first 2 s, with a greater amplitude than that of relative humidity, and the saltation sublimation rate increases with time. However, the mass of saltating particles basically stays unchanged after 2 s, while the relative humidity near the surface gradually increases. Therefore, the sublimation rate decreases with time. The relative humidity near the surface also reaches steady state after 300 s, resulting in stability of the sublimation rate. The saltating particles are distributed mainly near the surface, where the amplitude change of relative humidity is strong, resulting in a strong negative feedback effect on saltating particles.
It is shown in Fig. 9b that the sublimation rate of suspended particles increases with time and finally stabilizes at about 300 s. The negative feedback effect on suspended particles is not obvious. The mass of suspended particles increases with time during the first 300 s with an amplitude larger than that of the relative humidity. So the suspended sublimation rate increases with time. Then the mass of suspended particles and relative humidity both reach their steady states, leading to the sublimation rate of suspended particles becoming constant. Since the suspended particles are mainly distributed in the upper air where the amplitude change of relative humidity is weak, therefore the negative feedback effect on suspended particles is also weak.
Although the effect of negative feedback on saltating particles is stronger than that on suspended particles, the sublimation rate of saltating particles is still greater than that of suspended particles, indicating that the sublimation of saltating particles is very strong even under the effect of negative feedback.
Vertical profiles of mass concentration for saltation and
suspension:
Figure 10 shows that the mass concentration of snow particles increases with friction velocity and decreases with height, and the mass concentration of saltating particles is much higher than that of suspended particles. It can be seen from Fig. 10a that saltating particles are mainly distributed at height below 0.1 m, which is consistent with the previous experimental results (Takeuchi, 1980).
Vertical profiles of sublimation rate for saltation and
suspension:
Figure 11 shows that sublimation rates increase with friction velocity. The sublimation rates of saltating and suspended particles show a decreasing trend after increasing and reaching a peak at about 0.01 m for saltating particles, and about 0.1 m for suspended particles. This is because the mass concentration and relative humidity of snow particles decrease with height, while temperature increases. However, the mass concentration of saltating particles changes more strongly than that of suspended particles with height. Therefore, the sublimation rate of saltating particles reaches a peak at lower height.
Sublimation rate at 1500 s for snow particles at various heights.
Table 2 shows that the sublimation rate at 0.01 m is 2 orders of magnitude faster than that at 0.1 m, consistent with the experimental results in Fig. 3, and 3–4 times faster than that at 10 m, although the negative feedback effect near surface is stronger than in other regions. Because the mass concentration of snow particles near surface is much higher than that in other regions (Fig. 8), and water vapour near surface is not saturated, the sublimation rate near surface is much faster than that in other regions.
The ratio of sublimation mass below three heights to the total. Sublimation mass below a certain height is the sublimation mass that was ignored by other models (Déry et al., 1998; Pomeroy and Male, 1992, and Xiao et al., 2000).
The snow sublimation near surface was ignored in most previous studies (Déry et al., 1998; Xiao et al. 2000; Vionnet et al., 2014). That is, to define a wind-velocity-related height below which saltating particles move, saltating particles are moved due to wind velocity below a certain height. Assuming that moisture below the height is saturated, therefore the snow sublimation would not be counted in the region (Déry et al., 1998; Xiao et al., 2000; Vionnet et al., 2014). The heights at three wind velocities proposed by Déry et al. (1998), Pomeroy and Male (1992), and Xiao et al. (2000) are given in Table 3 (the heights of Vionnet et al. (2014) were the same as those of Pomeroy and Male, 1992). Figure 12 shows the actual ratio of our simulated sublimation mass below the three heights to the total. It is clear that all the sublimation masses below the three heights account for more than half of the total sublimation mass. This is because the main part of snow particles is composed of saltating particles (Mellor, 1965), which are mainly distributed in the near-surface region. Although sublimation near the surface leads to significant changes in temperature and humidity, which have a strong inhibition effect on sublimation, moisture near the surface does not reach saturation due to the vertical diffusion of water vapour, resulting in continuous snow sublimation. Therefore, the main part of the sublimation mass is sublimation of saltating particles. Thus, it is not appropriate to neglect blowing snow sublimation near the surface as in previous reported methods (Déry et al., 1998; Xiao et al., 2000; Vionnet et al., 2014). Figure 12 also shows that the proportion of the sublimation mass near the surface decreases with friction velocity. Because more snow particles can enter into the upper air with increased wind velocity, which will lead to a decrease in the proportion of snow particles near the surface, the proportion of the sublimation mass near the surface will decrease as well.
The height below which most of the saltating particles were distributed at various friction velocities.
Vertical profiles of vapour flux.
Figure 13 shows the vertical profiles of vapour flux. It is clear that vapour flux increases rapidly in the near-surface region, where most of saltating particles move, and slows down greatly after reaching a certain height. Because there is no horizontal flux of water vapour, the water vapour flux at any height must be equal to the total amount of water vapour generated per second below the height. So most of the water vapour is coming from near-surface regions. It also can be seen from Fig. 13 that vapour flux increases with friction velocity, similar to the behaviour for humidity (Fig. 5) and the moisture diffusion coefficient (Eq. 17).
We have established a blowing snow sublimation model with consideration of vertical moisture diffusion and heat balance, to study snow sublimation near the surface in large snow-covered areas in this paper. The simulation results show that the blowing snow sublimation decreases air temperature while it increases air humidity. Meanwhile, the snow sublimation is reduced by the negative feedback effect of temperature and humidity, especially in the near-surface region, in agreement with previous researches. However, moisture near the surface is not saturated due to the vertical moisture diffusion, so snow sublimation near the surface is a continuous process. The sublimation rate near the surface is even larger than that in the upper air, because the mass concentration of snow particles near the surface is much higher than that in other regions. The sublimation rate at 0.01 m is 2 orders of magnitude greater than that at 0.1 m, and is 3–4 orders of magnitude greater than that at 10 m. Furthermore, at low wind speed, the mass of sublimation near the surface accounts for more than half of the total sublimation mass, and cannot be neglected. Most of the air vapour in blowing snow is from the near-surface region. Therefore, blowing snow sublimation near the surface should be taken seriously in the study of snow sublimation and water vapour transport in the future.
We will continue to develop our model. Two possible improvements are (1) to extend the model to three dimensions and take into consideration the effects of turbulence on the sublimation of both saltating and suspended particles in the atmospheric turbulent boundary layer, which will lead to a more accurate and realistic model, and (2) to propose a parametric model of the blowing snow sublimation, which will provide parameterized values for the mesoscale climate model of polar ice sheet, alpine glacier, snowy areas at high latitude, and so on.
The data can be obtained by contacting the corresponding author.
The authors declare that they have no conflict of interest.
This work is supported by the State Key Programme of the National Natural Science Foundation of China (91325203), the National Key Research and Development Programme of China (2016YFC0500900), and the Innovative Research Groups of the National Natural Science Foundation of China (11121202). Edited by: Philip Marsh Reviewed by: Ally Toure and three anonymous referees