# The Effects of Sandstorms on the Climate of Northwestern China

Authors: Tiantian Hu; Di Wu; Yaohui Li; Chenghai Wang
Journal: Advances in Meteorology
 (2017)

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## Abstract

In this paper, we investigate the observational direct radiation characteristics of several sandstorm events in Northwestern China (NWC). A simulating sensitivity experiment was designed to reduce the downward radiation in RegCM4 to investigate the climatic impacts and persistence of the direct radiation effect (DRE) from dust aerosols in sandstorms. The results show that dust aerosols in sandstorms can change the radiation heating rate of the atmosphere, heating the air in the middle and low troposphere and cooling Earth’s surface. The climate effects of continuous and intense sandstorms in April in NWC can reach downstream areas such as Southeast and Northeast China and can persist for months. The dust aerosols in sandstorms can enhance diabatic heating and moisture loss. Therefore, dust storms lead to the environment in NWC becoming warmer and dryer. Through analysis of the dust tracer total burden, we identified that the enhancement of the dust total burden in the arid region illustrated that the DRE of dust aerosol in sandstorm process can react with the dust emission, thus forming a self-feedback loop. The DRE can persist three months.


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## Body

## 1. Introduction

With the expansion of desertification, sandstorm activities occur more frequently [1]. Mineral dust is the most important component of natural aerosols, with 1000–4000 Tg of dust emitted every year [2]. Research has suggested that dust aerosol has strong impacts on regional climate through changing the radiative forcing [3]. The positive anomalies of dust are associated with a considerable reduction in surface shortwave radiation [4, 5], the surface is cooled, and the atmosphere is heated by the backscatter of dust aerosols [6].In general, the climate effects of dust aerosols can be divided into 3 categories: the direct radiation effect (DRE) occurs through scattering and absorbing solar direct radiation; the indirect effect of climate is where the aerosols act as cloud condensation nuclei or ice nuclei, thus changing the microphysics and optical properties as well as the precipitation efficiency of cloud (cloud reflection and ice nucleation effects); and the semidirect effect occurs when the strong absorption of radiation of aerosols (such as soot) releases thermal radiation following the prior absorption of solar radiation energy, thus heating the air mass and increasing the static stability relative to the surface. This can also lead to cloud droplet evaporation and cause a decrease in cloud cover and cloud albedo, thus affecting the climate [7]. Kaspari et al. (2009) used ice cores to analyze the sources and variations in atmospheric dust from 1650 to 2002 and suggested that the chemical composition of dust varies seasonally, and peak dust concentration occurs during the winter and spring months [8].Seinfeld et al. (2004) examined ACE-Asia in situ measurements and found that the single-scatter albedo of pure dust’s diameter at 500 nm is 0.98 [9]. This suggests the dust changes the shortwave radiation, mainly though scatter. Northwest China (NWC) has areas covered by the Gobi Desert and loess regions, which are major source regions of Asian dust. Zhao et al. (2015) used an aerosol-climate coupled system to investigate the direct climatic effects of dust aerosol on global arid and semiarid regions and concluded that the cooling effects of dust aerosols can lead to anomalies in evaporation, circulation, and global precipitation [10]. During sandstorm events, the temperature and relative humidity in the atmosphere are changed, which affects atmospheric stratification features and precipitation.Wang et al. (2013) used the Weather Research and Forecasting (WRF) model to simulate the occurrence of a dust storm in Northern China during April 22–25, 2009, and suggested that the diabatic heating effect plays an important role in the sandstorm development and maintenance [11]. The simulation with RegCM4 shows that dust aerosols might increase the wet season precipitation in the Arabian Peninsula; the dust plumes exert a negative (positive) radiative forcing at the surface (top of the atmosphere) by reducing incoming solar radiation, reaching the ground and locally heating up the atmospheric column [12]. Using coupled and uncoupled dust experiment with RegCM4, Sun et al. (2012) analyzed the spatiotemporal distribution of dust aerosols and their climatic impact though direct radiation forcing over East Asia and found that dust aerosol-induced cooling leads to the formation of a cyclonic circulation in the middle and lower troposphere in NWC that further excites downstream an anticyclonic circulation (the Yellow River Loop) and a cyclonic circulation (East China Sea, ECS) [13].Most of the studies investigated the climate effects of the dust aerosols by considering radiation. The radiative forcing caused by dust aerosols in sandstorms can cause local surface temperature decreases and form a regional cold source. Usually, there are 3–5 sandstorms in NWC in spring every year and each sandstorm lasts for 3–5 days. It remains uncertain what the major changes are in the atmospheric stratification during a sandstorm process, what climatic effects are associated with continuous heavy sandstorms process in a month, how long such climate effects persist, which climatic changes may be caused in downstream areas, and what their extent may be. Furthermore, the potential subsequent effect on future dust emissions is also uncertain. Answering these questions will improve our understanding of the impacts and mechanisms behind dust storms. This paper will investigate the impacts of the DRE of dust aerosols in sandstorms on the environment in NWC. In Section2, the observed global and DRE characteristics during sandstorms are presented. The data and model descriptions and experimental design in this study are provided in Section 3. The DRE of dust aerosols in sandstorms in NWC are illustrated in Section 4. Section 5 provides a summary and conclusion.


## 2. The Observational Characteristics of Radiation Changes during Sandstorms

Sandstorms cause entrainment of sand mass into the air, leading to the sharp decrease of radiation flux in the atmosphere near the surface and reducing the local temperature; such persistent cooling will cause the region to become a cold source [14]. The soil dust aerosols redistribute heating from the surface to within the dust layer [15]. Table 1 shows the radiation changes observed in sandstorm events that have occurred in NWC. On the desert sunny days, because the cloud cover is low and the air is clean, dust aerosols only marginally influence solar radiation reduction in the air and a large amount of global radiation can reach the surface. However, during sandstorm weather, the abundant dust source and dry surface in the desert provide optimum conditions for dust emission and the high dust concentration in the air rapidly reduces direct radiation. For example, at the Tengger Desert experimental station (37°28′N, 105°01′E), during April to September in 2001, it was observed that the solar radiation reduction during dust weather reached about 10–90% and the average attenuation was about 38% [16]. During 2 sandstorms that occurred in the Taklimakan Desert hinterland (38°58′N, 83°39′E) on April 10, 2006, [17] and April 22, 2007 [18], the global radiation reduced about 94.5% and 59%, respectively. Kong et al. (2008) summarized that the observed net radiation during sandstorms in the Taklimakan Desert reduced about 50% on average [18].Table 1
The radiation force of aerosols in sandstorms cases.
Time
Location
Radiation
Reference
From April to September, 2001
Tengger Desert;(37°27′535′′N, 105°00′643′′E, altitude 1339 m)
The global radiation reduced 10–90% in sand and dust weather; average attenuation is about 38%.
Xin et al. (2003) [16]
April 10, 2006
Taklimakan Desert;(83°40′E, 39°N, altitude 1099.3 m)
The global radiation reduced 94.5%.
Li et al. (2011) [17]
April 22, 2007
Taklimakan Desert hinterland(83°39′E, 38°58′N, altitude 1099.3 m)
Global radiation reduced by 59%; the average dust radiation force in Taklimakan Desert is about 50% during the observation.
Kong et al. (2008) [18]
April 23, 1991
Desert station near Zhangye;(39°26′N, 100°12′E)
The surface global radiation reduced 83.1 W m−2.
Shen and Wei (2000) [19]
April 23, 1991
Zhangye Station;(38°50′N, 100°23′E)
The surface global radiation reduced 60.0 W m−2.
Shen and Wei (2000) [19]
March 27, 2004
Beijing
The global radiation reduced 37.8% during the sandstorm.
Hu et al. (2005) [20]However, in the NWC semiarid region, because of the different geological structure, the vegetation cover on the underlying surface, and the influence of the surrounding terrain, the intensity of wind is weaker and the burden of sand is low compared with the desert; therefore, a reduction of radiation by dust aerosols is also different compared with the desert area [19]. The Hexi Corridor in NWC is a high incidence area of sandstorms, blowing sand, and floating dust. For example, from the last ten days of February to the first ten-day period of May 1991, there were 11 observed sandstorms in Zhangye Station (38°50′N, 100°23′E) and the adjacent desert station (39°26′N, 100°12′E) and the air was continually muddy during that period. On April 23 (a muddy day), the 2 stations measured higher planetary albedo, compared with clear days and, on muddy days, the observed surface global radiation reduced 60.0 W m−2 and 83.1 W m−2 at the Zhangye and desert stations, respectively [19]. Similar cooling effects occurred in East China; even though this region is far away from the sand source, it is also subject to frequent sandstorm activity. During a sandstorm observed in Beijing on March 27, 2004, the global radiation reduced 37.8% of a clear day [20].Studies have suggested that the frequency of sandstorms is increasing in Northwest China (NWC) in recent years [21, 22]. Figure 1 shows the inter-decadal change in sandstorm frequency in NWC from 1950 to 2000; the sandstorm occurrence frequency was 5 times per year during 1950–1960 and then increased sharply every 10 years, reaching 23 times per year during 1990–2010. It is worth noting that Figure 1 only shows the sandstorm frequency in NWC during 1950–2000; however, some researches suggested that sandstorm occurrence days show a decreasing trend from 1950 to 2000 in the whole China and East Asia, as well as several stations in NWC [23–25]. It is not conflicting because of the difference of statistical method. According to the sandstorm occurrence frequency statistics in spring during 2004 to 2012 at 5 provincial capital cities in NWC (Table 2), sandstorms occurred every spring, especially in March and April from 2004 to 2012 (the position of the 5 provincial capital cities is shown in Figure 2). Otherwise, sandstorms occurred in Urumchi almost half of the years between 2004 and 2012. The number of sandstorm days at Urumchi is 1.4 days per year during the 9 years (2004–2012). The maximum number of sandstorm days occurs in Yinchuan, at 21.9 dust storm days per year on average in the 9 years. In Lanzhou, dust storms occurred 7.6 days per year on average; otherwise, Yinchuan and Lanzhou are located downstream of the main dust source.Table 2
The frequency of sandstorm at the five provincial capital cities in NWC from 2004 to 2012 (day a−1).
City
Total days
Days in March
Days in April
Days in May
Days in June
Xian
6.0
0.7
0.7
0.5
0.0
Lanzhou
7.6
2.8
2.7
1.4
0.2
Xining
1.5
0.3
1.0
0.0
0.0
Yinchuan
21.9
3.3
3.9
1.8
0.2
Urumchi
1.4
0.0
0.8
0.2
0.0Figure 1
Inter-decadal change in sandstorm frequency in NWC between 1950 and 2000.Figure 2
The five stations in provincial capital cities, as presented in Table2 (black points), and the domain of the RegCM4 simulation. Shading denotes surface model elevation (m).Table3 shows the radiation flux changes in 5 sandstorm processes during 2009 to 2011 from observed data at Lanzhou Station (36°03′N, 103°53′E). The observed data is 12 h of radiation exposure. The reduction of the global radiation during the sandstorm process is substantial due to the sandstorm strength. In 5 sandstorm processes, the global radiation decreasing rate ranges from 4% to 36%; on average, the decrease is 21%.Table 3
Radiation flux changes in five sandstorm processes in Lanzhou during 2009 to 2011.
Sandstorm date
Global radiation (MJ m−2)
Clear sky date
Global radiation (MJ m−2)
Decrease rate
09/04/2009
235
05/04/2009
322
0.27
24/04/2009
236
20/04/2009
320
0.26
19/03/2009
266
16/03/2009
277
0.04
09/04/2010
275
30/04/2010
299
0.08
29/04/2011
202
05/05/2011
318
0.36
Average
242.8
307.2
0.21Figure3 shows the change in the ground meteorological elements and radiation during a dust weather process in Lanzhou from April 23 to 24, 2009, using the observed data at Lanzhou Station (36°03′N, 103°53′E). The 6-hour visibility sharply decreased at 14:00 (LZT) April 23, which indicates the strongest level of dust concentration (Figure 3(a)). The visibility was only 200 m at this time and it remained lower than 500 m from 20:00 (LZT) April 23 to 2:00 (LZT) April 24, which indicates that the polluted air persisted for at least 12 hours. The global radiation reached a minimum value at 12:00 (LZT) April 23 and the irradiance was only 113.9 W m−2. In contrast, at the same time on April 24, the irradiance was 655.6 W m−2, indicating that the global radiation reduces 82% during the sand process. The wind speed sharply decreased near 14:00 (LZT) on April 23 and the wind direction turned from the northeast to the southeast (Figure 3(b)). After 17:00 (LZT) on April 23, the wind speed increased considerably. The pressure decreased at around 14:00 (LZT) on April 23, while the temperature increased during that period (Figure 3(c)). The air pressure increased and the temperature decreased at 18:00 (LZT) at sunset on April 23.Figure 3
Evolution of the observational elements from April 23 to 24, 2009 (BJT). (a) 6-hour visibility and irradiance; (b) hourly wind speed and wind direction; (c) air pressure and temperature.
(a)
(b)
(c)Above observations show that, on average, the amount of global radiation arriving at Earth’s surface will reduce during sandstorm events with an average reduction of about 20–60%. The month with the highest frequency of sandstorms is usually April in NWC.


## 3. Model Description and Experiment Design

This work employs the regional climate model version 4.4 (RegCM4.4), with the chemical module working, which was developed by the Abdus Salam International Centre for Theoretical Physics (ICTP). The model is fully described in a special issue of Climate Review [28]. The model has σ vertical coordinates and the whole atmosphere is divided into 18 layers. The domain of simulation is given in Figure 2. The center of the lattice is 35°N, 100°E and the horizontal resolution is 50 km (Table 4). We use the European Centre for Medium-Range Weather Forecasts Interim (ERA-Interim) dataset to drive RegCM4 [29]. The radiation scheme in the model is from National Center for Atmospheric Research (NCAR) Community Climate Model version 3 (CCM3), which is described in Kiehl et al. (1996) [30]. For this simulation, we selected the Biosphere-Atmosphere Transfer Scheme (BATS) [31] for surface process representation, the Emanuel (1991) scheme [27] as the cumulus convection parameterization scheme, and the Holtslag (1990) scheme [26] as the planetary boundary layer scheme and used the relaxation, exponential technique for the lateral boundary conditions scheme. The dust chemical tracers were activated in the model using four kinds of dust bins scheme. The mineral dust simulation of RegCM4.4 is described by Laurent et al. (2008) [32] and Alfaro and Gomes (2001) [33]. The 4 bins calculate the emission and tracer of dust aerosols at 0.01, 1.00, 2.50, and 5.00 micrometers particle diameter.Table 4
Details of the regional climate model version 4.4 (RegCM4.4) scheme.
Term
Scheme
Center of lattice
35°N, 100°E
Horizontal resolution
50 km
Time steps
100 s
Lateral boundary condition scheme
Relaxation, exponential technique
Boundary layer scheme
Holtslag [26]
Cumulus convection scheme
Emanuel [27]
Ocean flux scheme
Zeng
Land surface model
Biosphere-Atmosphere Transfer Scheme (BATS)
Chemistry scheme
Dust


### 3.1. Radiation Parameterization Schemes

The RegCM4 model uses the radiation scheme of NCAR CCM3, which uses theδ-Eddington approximation when calculating the solar radiation. A similar derivation of the downward flux is straightforward. The resulting expressions for the upward and downward flux are as follows:(1)Fup=e-τ∗/μ0Rupμ0+Tdnμ0-e-τ∗/μ0R-up1-R-dnR-up,Fdn=e-τ∗/μ0+Tdnμ0-e-τ∗/μ0+e-τ∗/μ0Rupμ0R-dn1-R-dnR-up,where e-τ∗/μ0 is the direct beam transmission from top of atmosphere to the interface (τ∗ is the scaled optical depth from top of atmosphere to the interface), Rupμ0 is the reflectivity of atmosphere to the interface, Tdnμ0 is the total transmission to direct solar radiation incident from above to the entire atmosphere above the interface, R-up is the reflectivity of atmosphere below the interface to diffuse radiation from above, and R-dn is the reflectivity of atmosphere above the interface to diffuse radiation from below.The upward and downward spectral fluxes at each interface are summed to evaluate the spectrally integrated fluxes and then differenced to produce the solar heating rate:(2)Qsol=gcpFdnpk+1-Fuppk+1-Fdnpk+Fuppkpk+1-pk.This is added to the nonlinear term (Q) in the thermodynamic equation.Vertical distribution of aerosols has a great impact on the heating rate profile, which provides more details about dust aerosol DRE on different atmospheric levels than radiation force. Over the Taklimakan Desert, dust aerosols can heat the atmosphere by up to 1, 2, and 3 K d−1 (daily mean values) under light, moderate, and heavy dust conditions, respectively; the maximum daily mean of radiative heating rate can reach 5.5 K d−1 at 5 km, at the location of the dust layer [34].


### 3.2. Sensitivity Experiment Design

In order to investigate the climate effects of dust aerosols in arid regions, a control experiment (CE) was established in which there were no changes during the whole integration. A sensitivity experiment (SE) was designed as follows: as mentioned in Section2, the amount of global radiation arriving at Earth’s surface will reduce during sandstorm events with an average reduction of about 20–60%; the SE adopted the middle value of 40% to reduce downward radiation flux every April from 2001 to 2010 in the region of 37.5°–47.5°N, 70°–105°E, where the sandstorm is frequent (Figure 4). The downward radiation flux is reduced 5% per layer in the 8 boot layers of the σ vertical coordinate, which corresponds with around 700 hPa. The altitude of the eighth layer is about 2 km; therefore, the downward radiation reaching the surface is only around 60%. Because of the changing downward shortwave radiation fluxes, Qsol enhanced subsequently in response to the effects of scattered radiation, thus heating the air.Figure 4
Difference of surface net downward shortwave radiation flux (W m−2) between sensitivity experiment (SE) and control experiment (CE) in April averaged from 2001 to 2010.The simulation time was from 01 January 2001 to 01 March 2011. In particular, the first 2 months were regarded as the spin-up period, and the results from 01 March 2001 to 01 March 2011 were used for analysis.To validate the performance of the RegCM4.4 model for the simulation in China, Figure5 shows the comparison of the precipitation and temperature between simulated results in CE and observed data from 668 weather stations in China. Compared to Figures 5(a) and 5(c), Figures 5(b) and 5(d) indicate that the model can reproduce the basic distribution characteristics of 2 m temperature and precipitation in China. The 2 m temperature in simulation in most of the regions in China is about 1-2°C lower than observational data except in high and complex terrain. The simulation reproduces the precipitation distribution in China (Figure 5(d)), except in southwest China. The number of observational stations is relatively sparse in Tibetan Plateau which may cause the observed biases. Therefore, the model used in this study has a good performance and can be used for the SE.Figure 5
Comparison of mean temperature and precipitation averaged from 1 March 2001 to 1 March 2011 between observation and simulation. (a) Observed 2 m temperature (K) from 668 stations; (b) observed precipitation (mm/d) from 668 stations; (c) simulated 2 m temperature (K); (d) simulated precipitation (mm/d); (e) differences of 2 m temperature (K); and (f) differences of precipitation (mm/d) between simulation and observation (simulation – observation).
(a)
Obs: 2 m temperature (K)
(b)
Obs: precipitation (mm/d)
(c)
CE: 2 m temperature (K)
(d)
CE: precipitation (mm/d)
(e)
CE − Obs: 2 m temperature (K)
(f)
CE − Obs: precipitation (mm/d)


## 3.1. Radiation Parameterization Schemes

The RegCM4 model uses the radiation scheme of NCAR CCM3, which uses theδ-Eddington approximation when calculating the solar radiation. A similar derivation of the downward flux is straightforward. The resulting expressions for the upward and downward flux are as follows:(1)Fup=e-τ∗/μ0Rupμ0+Tdnμ0-e-τ∗/μ0R-up1-R-dnR-up,Fdn=e-τ∗/μ0+Tdnμ0-e-τ∗/μ0+e-τ∗/μ0Rupμ0R-dn1-R-dnR-up,where e-τ∗/μ0 is the direct beam transmission from top of atmosphere to the interface (τ∗ is the scaled optical depth from top of atmosphere to the interface), Rupμ0 is the reflectivity of atmosphere to the interface, Tdnμ0 is the total transmission to direct solar radiation incident from above to the entire atmosphere above the interface, R-up is the reflectivity of atmosphere below the interface to diffuse radiation from above, and R-dn is the reflectivity of atmosphere above the interface to diffuse radiation from below.The upward and downward spectral fluxes at each interface are summed to evaluate the spectrally integrated fluxes and then differenced to produce the solar heating rate:(2)Qsol=gcpFdnpk+1-Fuppk+1-Fdnpk+Fuppkpk+1-pk.This is added to the nonlinear term (Q) in the thermodynamic equation.Vertical distribution of aerosols has a great impact on the heating rate profile, which provides more details about dust aerosol DRE on different atmospheric levels than radiation force. Over the Taklimakan Desert, dust aerosols can heat the atmosphere by up to 1, 2, and 3 K d−1 (daily mean values) under light, moderate, and heavy dust conditions, respectively; the maximum daily mean of radiative heating rate can reach 5.5 K d−1 at 5 km, at the location of the dust layer [34].


## 3.2. Sensitivity Experiment Design

In order to investigate the climate effects of dust aerosols in arid regions, a control experiment (CE) was established in which there were no changes during the whole integration. A sensitivity experiment (SE) was designed as follows: as mentioned in Section2, the amount of global radiation arriving at Earth’s surface will reduce during sandstorm events with an average reduction of about 20–60%; the SE adopted the middle value of 40% to reduce downward radiation flux every April from 2001 to 2010 in the region of 37.5°–47.5°N, 70°–105°E, where the sandstorm is frequent (Figure 4). The downward radiation flux is reduced 5% per layer in the 8 boot layers of the σ vertical coordinate, which corresponds with around 700 hPa. The altitude of the eighth layer is about 2 km; therefore, the downward radiation reaching the surface is only around 60%. Because of the changing downward shortwave radiation fluxes, Qsol enhanced subsequently in response to the effects of scattered radiation, thus heating the air.Figure 4
Difference of surface net downward shortwave radiation flux (W m−2) between sensitivity experiment (SE) and control experiment (CE) in April averaged from 2001 to 2010.The simulation time was from 01 January 2001 to 01 March 2011. In particular, the first 2 months were regarded as the spin-up period, and the results from 01 March 2001 to 01 March 2011 were used for analysis.To validate the performance of the RegCM4.4 model for the simulation in China, Figure5 shows the comparison of the precipitation and temperature between simulated results in CE and observed data from 668 weather stations in China. Compared to Figures 5(a) and 5(c), Figures 5(b) and 5(d) indicate that the model can reproduce the basic distribution characteristics of 2 m temperature and precipitation in China. The 2 m temperature in simulation in most of the regions in China is about 1-2°C lower than observational data except in high and complex terrain. The simulation reproduces the precipitation distribution in China (Figure 5(d)), except in southwest China. The number of observational stations is relatively sparse in Tibetan Plateau which may cause the observed biases. Therefore, the model used in this study has a good performance and can be used for the SE.Figure 5
Comparison of mean temperature and precipitation averaged from 1 March 2001 to 1 March 2011 between observation and simulation. (a) Observed 2 m temperature (K) from 668 stations; (b) observed precipitation (mm/d) from 668 stations; (c) simulated 2 m temperature (K); (d) simulated precipitation (mm/d); (e) differences of 2 m temperature (K); and (f) differences of precipitation (mm/d) between simulation and observation (simulation – observation).
(a)
Obs: 2 m temperature (K)
(b)
Obs: precipitation (mm/d)
(c)
CE: 2 m temperature (K)
(d)
CE: precipitation (mm/d)
(e)
CE − Obs: 2 m temperature (K)
(f)
CE − Obs: precipitation (mm/d)


## 4. The Climate Effects of Sandstorms

### 4.1. Temperature

Because of the reduction of downward radiation in SE, that is, during sandstorm processes, the reduced radiant energy transforms into thermal energy and stays in the atmosphere. This changes the heating rate of the atmospheric stratification, causing the air temperature in experiment region to increase at this time. The difference (DIF) of air temperature (SE − CE) in April NWC at 700 hPa (Figure6(b)) is the largest, compared with 2 m height (Figure 6(a)) and at 500 hPa (Figure 6(c)). This is because the height of 700 hPa is near the eighth layer of the σ coordinate, where heat accumulates. Because less downward radiation reaches Earth’s surface, the surface becomes a cold source in sandstorms and emits less longwave radiation to heat the tropopause. The temperature DIF (SE − CE) in April NWC becomes negative at 200 hPa (Figure 6(d)). At the heights of 2 m and 700 hPa in April, the area of temperature increase extends from NWC to Northeast and Southwest China, because of the transport of warm air by the wind from the north and west.Figure 6
The temperature DIF (SE − CE; K) at the height of (a) 2 m, (b) 700 hPa, (c) 500 hPa, and (d) 200 hPa in April averaged from 2001 to 2010.
(a)
(b)
(c)
(d)


### 4.2. Atmospheric Stratification

Figure7 shows the skew-T stratification curve during an observed sandstorm process at Minqing station (38°38′N, 103°05′E) which is included in NWC (37.5°N–47.5°N, 70°E–105°E), on April 24, 2010. The observed dust storm occurred at 12:00 UTC (20:00 LZT) at that station (Shen et al. 2014). At 00:00 UTC (8:00 LZT) (Figure 7(a)), the dew point temperature is higher below 400 hPa, indicating that the moisture is greater in SE than in CE in the morning, but the air temperature is lower in SE below 700 hPa near the surface at morning. This is because the cold effects from the surface dominate the lower atmosphere before sunrise. There was a substantial difference in air temperature in SE from 700 hPa to 400 hPa, relative to CE at the same heights, because of the heating effects of the dust aerosols. At 06:00 UTC (14:00 LZT) (Figure 7(b)), the temperature is higher in SE than in CE from the surface to around 700 hPa, and the moisture presents lower in SE between 700 hPa and 250 hPa than CE, which reverses above 250 hPa in the afternoon. At 12:00 UTC (20:00 LZT) (Figure 7(c)), when the observed sandstorm occurred, the temperature is higher in SE than in CE while the moisture is lower in SE than in CE, especially below 400 hPa in the evening. At 18:00 UTC (2:00 LZT) (Figure 7(d)), the moisture is still lower and the temperature is higher in the SE than in CE, but the DIF of temperature seems smaller at night compared with the evening. During the observed sandstorm process (Figure 7(c)), the temperature profiles rose along the dry adiabat in the lower atmosphere; the moisture is lower and the temperature is higher in middle and lower troposphere at the sandstorm occurrence time, compared with Figures 7(a), 7(b), and 7(c). This demonstrates that the results of the SE are consistent with the observed facts.Figure 7
The atmospheric stratification curve at (a) 00:00, (b) 06:00, (c) 12:00, and (d) 18:00 (UTC) on April 24, 2009, in Minqing in China (42.5°N, 87.5°E) (solid line: CE; dotted line: SE).
(a)
2009_4_24_00
(b)
2009_4_24_06
(c)
2009_4_24_12
(d)
2009_4_24_18Figure8 shows the vertical profile of DIF (SE − CE) for regional average air temperature, shortwave radiation heating rate (Qrs), and longwave radiation heating rate (Qrl) in NWC (37.5°N–47.5°N, 70°E–105°E) from April to June, which illustrates that the temperature changes caused by dust storms can reach the tropopause. In April (Figure 8(a)), the distinct air temperature DIF (solid line) appears around 700 hPa, which implies that the main impact of the dust storm is the temperature increase at low-level atmosphere. This increase can reach to 300 hPa in the troposphere. This is consistent with the results from Figure 6. Above 300 hPa, with the increase of height, the DIF becomes negative (the air temperature is lower in dust storm processes at the tropopause). The negative value reaches its minimum at 150 hPa. The change curve of the temperature DIF value indicates a value of small magnitude in May (Figure 8(b)) and June (Figure 8(c)); that is, the change of air temperature in May and June is imperceptibly small. Even though the DIF is small, the air temperature DIF remains positive below 150 hPa and negative above 150 hPa in May and June (i.e., the air temperature increases about 0.1 K below 150 hPa and decreases about 0.1 K above 150 hPa in SE in May and June). In conclusion, the climate effects of dust storms in NWC in April can last to May and June; however, the intensity is weaker in the later months.Figure 8
The vertical profile of DIF (SE − CE) for regional averaged air temperature (K), shortwave heating rate (Qrs) (°C d−1), and longwave heating rate (Qrl) (°C d−1) in (a) April, (b) May, and (c) June, respectively, in NWC (37.5°N–47.5°N, 70°E–105°E) averaged from 2001 to 2010.
(a)
(b)
(c)


### 4.3. Radiation Heating Rate

Because the downward shortwave radiation has been reduced, the energy is retained in the atmosphere. TheQrs DIF (SE − CE) remains positive and decreases below 400 hPa in April (Figure 8(a), dashed line). For example, Qrs in sandstorm weather is higher than in non-sandstorm weather, which implies that the air at the low-level atmosphere is heated by the reduced radiation energy. Moreover, after reducing the downward radiation, less energy reached the surface, so the land becomes cooler and emits less longwave radiation energy. Qrl during the sandstorm is smaller than during non-sandstorm weather at below 600 hPa. The Qrl DIF (SE − CE) decreases with the height from the surface to 600 hPa in April (Figure 8(a), dotted line). The Qrl DIF (SE − CE) approaches 0 between 600 hPa and 100 hPa indicating that Qrl is reduced in dust storms in the lower levels of the atmosphere because of the cooling effects of the land, and the influence is decay with the height. Qrs and Qrl DIF in May (Figure 8(b)) and June (Figure 8(c)) are near to 0 because the reduction of downward shortwave radiation ceases. In contrast, in April (Figure 8(a)), the Qrs DIF is one order of magnitude larger than Qrl DIF (i.e., the heating effects of Qrs in the atmosphere are more important than the cooling effects of Qrl near the surface).


### 4.4. The Change of Heating

Based on the regional average of NWC (37.5°N–47.5°N, 70°E–105°E), the vertical profile of the apparent heat source (Q1) in April (Figure 9(a)) is maintained positive below 200 hPa and the value in SE (dashed line) is larger than in the CE (solid line) below 400 hPa. This indicates that the atmosphere below 200 hPa is a heat source and the DRE of dust aerosols in sandstorms enhances the diabatic heating effect below 400 hPa in SE. Q1 becomes negative above 200 hPa, indicating that the tropopause in April in NWC is a cold source. The apparent moisture sink (Q2) in NWC maintains a negative value in April (Figure 9(b)), which means that the moisture loss is more than moisture influx in the arid area. This phenomenon may be because of the high evaporation capacity in NWC (i.e., the same reason that arid conditions were formed). The DRE of the dust aerosols in sandstorms enhances the dry conditions indicated by the lower Q2 in SE than in CE. This is because the increase of air temperature may enhance the evaporation. In contrast, the magnitude of Q1 is one order of magnitude larger than Q2, which is due to the arid environment. Qrs is clearly enhanced in SE below 450 hPa and remains positive (Figure 9(c)) because the DRE of dust aerosols in sandstorms can enhance Qrs through enhancing the scattering of radiation, thus heating the air. However, Qrl is negative because of the cold source effect of the surface and is smaller below 650 hPa in SE than in CE (Figure 9(d)). This phenomenon highlights that the effects of the DRE of dust aerosols in sandstorms could enhance the cold source effects from the surface. The reason for the enhancement of Qrl between 650 hPa and 350 hPa is related to the enhancement of longwave radiation emitted from the low-level atmosphere because of the increase of air temperature in the low-level atmosphere. The above results show that the DRE of dust aerosols in sandstorms can enhance the heat source effects and dry conditions in NWC, through heating the air in the middle and low-level troposphere and enhancing the cold source effects of the surface.Figure 9
The vertical profile of (a) apparent heat source (Q1/(°C d−1)); (b) apparent moisture sink (Q2/(°C d−1)); (c) shortwave radiation heating rate (Qrs/(°C d−1)); (d) longwave radiation heating rate (Qrl/(°C d−1)) in SE and CE, respectively, in April averaged from 2001 to 2010.
(a)
Apparent heat source
(b)
Apparent moisture sink
(c)
Q
r
s
(d)
Q
r
l


### 4.5. The Changes of Water Vapor Flux

The DIF (SE − CE) distributions of 700 hPa relative humidity, 700 hPa water vapor flux, surface pressure, and 700 hPa specific humidity in April averaged from 2001 to 2010 are shown in Figure10. There were no clear changes in May and June (figures are omitted). In the NWC and south China, the relative humidity decreased considerably (Figure 10(a)). This is because the increased temperature led to an increase in the saturated vapor pressure point. In this case, the water vapor in the air becomes more difficult to coagulate. This effect may well correspond to the precipitation distribution during the sandstorm process in NWC. The change of the surface pressure is reflected more clearly in NWC and south China (Figure 10(c)); the rise of air temperature led to the swell of the air and thus led to the reduction of the surface pressure. The DIF (SE – CE) of water vapor flux field expresses changes in the ability of the air to transport water vapor (Figure 10(b)). Combined with the change of wind field, it clearly shows that the water vapor flux decreases north of the experimental region and increases south of the experimental region in SE. The wind can be seen to strengthen the convergence in the east of NWC and strengthen the divergence in the west of the experimental region. This possibly relates to the topographic condition and large scale circulation background; however, the change mechanisms of water vapor flux are complex and the mechanism causing the response requires further research. The DIF (SE – CE) distribution of 700 hPa specific humidity in air is consistent with the DIF (SE – CE) of the water vapor flux field; the specific humidity decreases in north NWC and increases in south NWC; however, these mechanisms are as complex as the water vapor flux and further research is required before they can be examined in further detail.Figure 10
(a) The DIF (SE − CE) of 700 hPa relative humidity (%); (b) 700 hPa water vapor flux (g s−1·hPa−1·cm−1); (c) surface pressure (hPa); and (d) 700 hPa specific humidity (g kg−1) in April averaged from 2001 to 2010.
(a)
Relative humidity
(b)
Water vapor flux
(c)
Surface pressure
(d)
Specific humidity


### 4.6. The Changes of Dust Tracer Total Burden

The analysis above emphasizes that the DRE of dust aerosols during a sandstorm in NWC could enhance the air temperature and reduce the moisture. For example, the environment in NWC will become warmer and dryer if sandstorms occur more frequently, last longer, and have a stronger intensity. Under these conditions, the climate effects of DRE in sandstorms may react to the emission of dust from the surface. Figure11 shows the DIF of tracer total burden of the 4 dust bins in RegCM4 in April, May, and June averaged from 2001 to 2010. The 4 dust bins in RegCM4 are used to calculate the emission and tracer of dust aerosols with 0.01-, 1.00-, 2.50-, and 5.00-micrometer particle diameter. The magnitude of the dust tracer total burdens indicates that the DIF (SE − CE) of the 0.01 and 5.00 micrometers size dust aerosols tracer burdens are largest in the simulation, the DIF (SE − CE) of 1.00 micrometers size aerosols tracer burden is in the middle, and the DIF (SE − CE) of 2.50 micrometers size aerosols tracer burden is the shortest. Combining the analysis, the burdens of the 4 different dust bins increase strongly in NWC in April, and they flow to downstream areas such as Northeast and Southwest China. This increase can last to May and June, although the increase is smaller in these later months.Figure 11
The DIF (SE − CE) of the tracer total burden (mg m−2) of the four dust bins (DUST01–DUST04) in April, May, and June averaged from 2001 to 2010.
(a)
April
(b)
May
(c)
June
(d)
April
(e)
May
(f)
June
(g)
April
(h)
May
(i)
June
(j)
April
(k)
May
(l)
June


## 4.1. Temperature

Because of the reduction of downward radiation in SE, that is, during sandstorm processes, the reduced radiant energy transforms into thermal energy and stays in the atmosphere. This changes the heating rate of the atmospheric stratification, causing the air temperature in experiment region to increase at this time. The difference (DIF) of air temperature (SE − CE) in April NWC at 700 hPa (Figure6(b)) is the largest, compared with 2 m height (Figure 6(a)) and at 500 hPa (Figure 6(c)). This is because the height of 700 hPa is near the eighth layer of the σ coordinate, where heat accumulates. Because less downward radiation reaches Earth’s surface, the surface becomes a cold source in sandstorms and emits less longwave radiation to heat the tropopause. The temperature DIF (SE − CE) in April NWC becomes negative at 200 hPa (Figure 6(d)). At the heights of 2 m and 700 hPa in April, the area of temperature increase extends from NWC to Northeast and Southwest China, because of the transport of warm air by the wind from the north and west.Figure 6
The temperature DIF (SE − CE; K) at the height of (a) 2 m, (b) 700 hPa, (c) 500 hPa, and (d) 200 hPa in April averaged from 2001 to 2010.
(a)
(b)
(c)
(d)


## 4.2. Atmospheric Stratification

Figure7 shows the skew-T stratification curve during an observed sandstorm process at Minqing station (38°38′N, 103°05′E) which is included in NWC (37.5°N–47.5°N, 70°E–105°E), on April 24, 2010. The observed dust storm occurred at 12:00 UTC (20:00 LZT) at that station (Shen et al. 2014). At 00:00 UTC (8:00 LZT) (Figure 7(a)), the dew point temperature is higher below 400 hPa, indicating that the moisture is greater in SE than in CE in the morning, but the air temperature is lower in SE below 700 hPa near the surface at morning. This is because the cold effects from the surface dominate the lower atmosphere before sunrise. There was a substantial difference in air temperature in SE from 700 hPa to 400 hPa, relative to CE at the same heights, because of the heating effects of the dust aerosols. At 06:00 UTC (14:00 LZT) (Figure 7(b)), the temperature is higher in SE than in CE from the surface to around 700 hPa, and the moisture presents lower in SE between 700 hPa and 250 hPa than CE, which reverses above 250 hPa in the afternoon. At 12:00 UTC (20:00 LZT) (Figure 7(c)), when the observed sandstorm occurred, the temperature is higher in SE than in CE while the moisture is lower in SE than in CE, especially below 400 hPa in the evening. At 18:00 UTC (2:00 LZT) (Figure 7(d)), the moisture is still lower and the temperature is higher in the SE than in CE, but the DIF of temperature seems smaller at night compared with the evening. During the observed sandstorm process (Figure 7(c)), the temperature profiles rose along the dry adiabat in the lower atmosphere; the moisture is lower and the temperature is higher in middle and lower troposphere at the sandstorm occurrence time, compared with Figures 7(a), 7(b), and 7(c). This demonstrates that the results of the SE are consistent with the observed facts.Figure 7
The atmospheric stratification curve at (a) 00:00, (b) 06:00, (c) 12:00, and (d) 18:00 (UTC) on April 24, 2009, in Minqing in China (42.5°N, 87.5°E) (solid line: CE; dotted line: SE).
(a)
2009_4_24_00
(b)
2009_4_24_06
(c)
2009_4_24_12
(d)
2009_4_24_18Figure8 shows the vertical profile of DIF (SE − CE) for regional average air temperature, shortwave radiation heating rate (Qrs), and longwave radiation heating rate (Qrl) in NWC (37.5°N–47.5°N, 70°E–105°E) from April to June, which illustrates that the temperature changes caused by dust storms can reach the tropopause. In April (Figure 8(a)), the distinct air temperature DIF (solid line) appears around 700 hPa, which implies that the main impact of the dust storm is the temperature increase at low-level atmosphere. This increase can reach to 300 hPa in the troposphere. This is consistent with the results from Figure 6. Above 300 hPa, with the increase of height, the DIF becomes negative (the air temperature is lower in dust storm processes at the tropopause). The negative value reaches its minimum at 150 hPa. The change curve of the temperature DIF value indicates a value of small magnitude in May (Figure 8(b)) and June (Figure 8(c)); that is, the change of air temperature in May and June is imperceptibly small. Even though the DIF is small, the air temperature DIF remains positive below 150 hPa and negative above 150 hPa in May and June (i.e., the air temperature increases about 0.1 K below 150 hPa and decreases about 0.1 K above 150 hPa in SE in May and June). In conclusion, the climate effects of dust storms in NWC in April can last to May and June; however, the intensity is weaker in the later months.Figure 8
The vertical profile of DIF (SE − CE) for regional averaged air temperature (K), shortwave heating rate (Qrs) (°C d−1), and longwave heating rate (Qrl) (°C d−1) in (a) April, (b) May, and (c) June, respectively, in NWC (37.5°N–47.5°N, 70°E–105°E) averaged from 2001 to 2010.
(a)
(b)
(c)


## 4.3. Radiation Heating Rate

Because the downward shortwave radiation has been reduced, the energy is retained in the atmosphere. TheQrs DIF (SE − CE) remains positive and decreases below 400 hPa in April (Figure 8(a), dashed line). For example, Qrs in sandstorm weather is higher than in non-sandstorm weather, which implies that the air at the low-level atmosphere is heated by the reduced radiation energy. Moreover, after reducing the downward radiation, less energy reached the surface, so the land becomes cooler and emits less longwave radiation energy. Qrl during the sandstorm is smaller than during non-sandstorm weather at below 600 hPa. The Qrl DIF (SE − CE) decreases with the height from the surface to 600 hPa in April (Figure 8(a), dotted line). The Qrl DIF (SE − CE) approaches 0 between 600 hPa and 100 hPa indicating that Qrl is reduced in dust storms in the lower levels of the atmosphere because of the cooling effects of the land, and the influence is decay with the height. Qrs and Qrl DIF in May (Figure 8(b)) and June (Figure 8(c)) are near to 0 because the reduction of downward shortwave radiation ceases. In contrast, in April (Figure 8(a)), the Qrs DIF is one order of magnitude larger than Qrl DIF (i.e., the heating effects of Qrs in the atmosphere are more important than the cooling effects of Qrl near the surface).


## 4.4. The Change of Heating

Based on the regional average of NWC (37.5°N–47.5°N, 70°E–105°E), the vertical profile of the apparent heat source (Q1) in April (Figure 9(a)) is maintained positive below 200 hPa and the value in SE (dashed line) is larger than in the CE (solid line) below 400 hPa. This indicates that the atmosphere below 200 hPa is a heat source and the DRE of dust aerosols in sandstorms enhances the diabatic heating effect below 400 hPa in SE. Q1 becomes negative above 200 hPa, indicating that the tropopause in April in NWC is a cold source. The apparent moisture sink (Q2) in NWC maintains a negative value in April (Figure 9(b)), which means that the moisture loss is more than moisture influx in the arid area. This phenomenon may be because of the high evaporation capacity in NWC (i.e., the same reason that arid conditions were formed). The DRE of the dust aerosols in sandstorms enhances the dry conditions indicated by the lower Q2 in SE than in CE. This is because the increase of air temperature may enhance the evaporation. In contrast, the magnitude of Q1 is one order of magnitude larger than Q2, which is due to the arid environment. Qrs is clearly enhanced in SE below 450 hPa and remains positive (Figure 9(c)) because the DRE of dust aerosols in sandstorms can enhance Qrs through enhancing the scattering of radiation, thus heating the air. However, Qrl is negative because of the cold source effect of the surface and is smaller below 650 hPa in SE than in CE (Figure 9(d)). This phenomenon highlights that the effects of the DRE of dust aerosols in sandstorms could enhance the cold source effects from the surface. The reason for the enhancement of Qrl between 650 hPa and 350 hPa is related to the enhancement of longwave radiation emitted from the low-level atmosphere because of the increase of air temperature in the low-level atmosphere. The above results show that the DRE of dust aerosols in sandstorms can enhance the heat source effects and dry conditions in NWC, through heating the air in the middle and low-level troposphere and enhancing the cold source effects of the surface.Figure 9
The vertical profile of (a) apparent heat source (Q1/(°C d−1)); (b) apparent moisture sink (Q2/(°C d−1)); (c) shortwave radiation heating rate (Qrs/(°C d−1)); (d) longwave radiation heating rate (Qrl/(°C d−1)) in SE and CE, respectively, in April averaged from 2001 to 2010.
(a)
Apparent heat source
(b)
Apparent moisture sink
(c)
Q
r
s
(d)
Q
r
l


## 4.5. The Changes of Water Vapor Flux

The DIF (SE − CE) distributions of 700 hPa relative humidity, 700 hPa water vapor flux, surface pressure, and 700 hPa specific humidity in April averaged from 2001 to 2010 are shown in Figure10. There were no clear changes in May and June (figures are omitted). In the NWC and south China, the relative humidity decreased considerably (Figure 10(a)). This is because the increased temperature led to an increase in the saturated vapor pressure point. In this case, the water vapor in the air becomes more difficult to coagulate. This effect may well correspond to the precipitation distribution during the sandstorm process in NWC. The change of the surface pressure is reflected more clearly in NWC and south China (Figure 10(c)); the rise of air temperature led to the swell of the air and thus led to the reduction of the surface pressure. The DIF (SE – CE) of water vapor flux field expresses changes in the ability of the air to transport water vapor (Figure 10(b)). Combined with the change of wind field, it clearly shows that the water vapor flux decreases north of the experimental region and increases south of the experimental region in SE. The wind can be seen to strengthen the convergence in the east of NWC and strengthen the divergence in the west of the experimental region. This possibly relates to the topographic condition and large scale circulation background; however, the change mechanisms of water vapor flux are complex and the mechanism causing the response requires further research. The DIF (SE – CE) distribution of 700 hPa specific humidity in air is consistent with the DIF (SE – CE) of the water vapor flux field; the specific humidity decreases in north NWC and increases in south NWC; however, these mechanisms are as complex as the water vapor flux and further research is required before they can be examined in further detail.Figure 10
(a) The DIF (SE − CE) of 700 hPa relative humidity (%); (b) 700 hPa water vapor flux (g s−1·hPa−1·cm−1); (c) surface pressure (hPa); and (d) 700 hPa specific humidity (g kg−1) in April averaged from 2001 to 2010.
(a)
Relative humidity
(b)
Water vapor flux
(c)
Surface pressure
(d)
Specific humidity


## 4.6. The Changes of Dust Tracer Total Burden

The analysis above emphasizes that the DRE of dust aerosols during a sandstorm in NWC could enhance the air temperature and reduce the moisture. For example, the environment in NWC will become warmer and dryer if sandstorms occur more frequently, last longer, and have a stronger intensity. Under these conditions, the climate effects of DRE in sandstorms may react to the emission of dust from the surface. Figure11 shows the DIF of tracer total burden of the 4 dust bins in RegCM4 in April, May, and June averaged from 2001 to 2010. The 4 dust bins in RegCM4 are used to calculate the emission and tracer of dust aerosols with 0.01-, 1.00-, 2.50-, and 5.00-micrometer particle diameter. The magnitude of the dust tracer total burdens indicates that the DIF (SE − CE) of the 0.01 and 5.00 micrometers size dust aerosols tracer burdens are largest in the simulation, the DIF (SE − CE) of 1.00 micrometers size aerosols tracer burden is in the middle, and the DIF (SE − CE) of 2.50 micrometers size aerosols tracer burden is the shortest. Combining the analysis, the burdens of the 4 different dust bins increase strongly in NWC in April, and they flow to downstream areas such as Northeast and Southwest China. This increase can last to May and June, although the increase is smaller in these later months.Figure 11
The DIF (SE − CE) of the tracer total burden (mg m−2) of the four dust bins (DUST01–DUST04) in April, May, and June averaged from 2001 to 2010.
(a)
April
(b)
May
(c)
June
(d)
April
(e)
May
(f)
June
(g)
April
(h)
May
(i)
June
(j)
April
(k)
May
(l)
June


## 5. Summary and Conclusion

Dust storms frequently occur in NWC, which leads to a hostile environment and weather. The pollution and cooling are well known; however, the influence extent and duration of the continuous sandstorms events are less understood and were investigated for NWC in this study. We specifically investigated the DRE from dust aerosols in sandstorms in the NWC region. Through combing simulations and observations, we described the basic radiation feature in the sandstorm as follows: the highest frequency month of sandstorms in NWC is in April, and the global radiation average reduces 20–60% during the sandstorm process. The RegCM4 (ICTP) was used to simulate the climate effects of dust aerosols in NWC from 01 January 2001 to 01 March 2011 with the first 2 months as the spin-up time. In SE, the downward shortwave radiation was reduced 40% in the bottom 8 layers inσ vertical coordinate which is equivalent to below 700 hPa every April to simulate the DRE of dust aerosols during sandstorms. The results show that the reduced shortwave radiation by dust aerosols can heat the middle and low troposphere and forms a cooler source at Earth’s surface, thus changing Qrs and Qrl. The air temperature below 300 hPa increases and that above 300 hPa decreases during sandstorms; the strongest enhancement is at about 700 hPa. Simultaneously, because of the short reach of shortwave radiation to the surface, the surface becomes a cold source and reduces the emission of longwave radiation. The change of the air temperature and surface conditions at NWC in April can affect the climate downstream in areas such as Northeast and Southwest China and last to May and June.Through analyzing the atmospheric stratification change during a sandstorm process in Minqin, we found that the short of downward radiation caused by dust storm can enhance the air temperature and reduce the moisture in the daytime in the middle and lower atmosphere. The analysis of the change in apparent heat source (Q1) and apparent moisture sink (Q2) in April and NWC shows that the conditions in NWC become warmer and dryer in SE during sandstorms. This suggests that the DRE of dust aerosols in sandstorms can enhance the heat source effects and cause the moisture loss in NWC. This is likely to cause an intensification of the drying trend. The changes of 700 hPa relative humidity, water vapor flux, surface pressure, and 700 hPa specific humidity further prove the points discussed above. We have found that the DRE of dust aerosols in sandstorms has a reaction on the dust aerosols emissions; that is, this effect could enhance the dust storm and form a self-feedback loop. These effects of sandstorms in April in NWC can flow to downstream areas such as Northeast and Southwest China and can last to May and June, but the intensity of the effects weakens in these later months.



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*Source: 4035609-2017-03-28.xml*