Summer dust aerosols detected from CALIPSO over the Tibetan Plateau

Authors


Abstract

[1] Summertime Tibetan dust aerosol plumes are detected from the Cloud-Aerosol Lidar and Infrared Pathfinder Satellite Observations (CALIPSO) satellite. CALIPSO reveals that dust storms occur more frequently than previously found from Tibetan surface observations because few surface sites were available over remote northwestern Tibet due to high elevation and harsh climate. The Tibetan dust aerosol is characterized by column-averaged volume depolarization and total volume color ratios around 21% and 0.83, respectively. The dust layers appear most frequently around 4–7 km above mean sea level. The volume depolarization ratio for about 90% of the dust particles is less than 10% at low altitudes (3–5 km), while only about 50% of the particles have a greater depolarization ratio at higher altitudes (7–10 km). The 4-day back trajectory analyses show that these plumes probably originate from the nearby Taklamakan desert surface and accumulate over the northern slopes of the Tibetan Plateau. These dust outbreaks can affect the radiation balance of the atmosphere of Tibet because they both absorb and reflect solar radiation.

1. Introduction

[2] Every year, deserts in eastern Asia produce a large amount of mineral dust particles that become entrained in the atmosphere. These particles have been recognized as important atmospheric constituents because dust particles influence the global climate by scattering and absorbing solar radiation, and absorbing and emitting outgoing long-wave radiation [Tegen, 2003; Huang et al., 2006b; Slingo et al., 2006]. They can also cause changes in cloud properties, such as the number concentration and size of cloud droplets, which can alter both cloud albedo and cloud lifetime [Twomey et al., 1984; Huang et al., 2006a].

[3] During the summer, dust from the deserts of western China, Afghanistan, Pakistan, and the Middle East is transported into and stacked up against the northern and southern slopes of the Tibetan Plateau. The absorption of solar radiation by dust heats up the elevated surface air over the slopes. Recently, Lau and Kim [2006] and Lau et al. [2006] pointed out that, on intra-seasonal to inter-annual time scales, heating by absorbing aerosols may induce a tropospheric temperature anomaly over parts of northern India and Tibet in late spring and early summer, leading to an earlier onset and intensification of the Indian monsoon. They proposed the importance of atmospheric heating by an “elevated heat pump” effect due to dust transported from the nearby deserts to northern India stacking up against the southern slopes of the Himalayas. This dust combined with the black carbon from industrial and agricultural pollution in northern India provides an anomalous diabatic heat source that triggers positive feedback in monsoon convective heating, enhancing the Indian monsoon. These results suggest that aerosol effects on the monsoon water cycle dynamics are complex and likely to be a strong function of spatial and temporal scales. However, no convincing evidence of aerosol effect on monsoon climate variability has been noted due to the lack of observed dust aerosol over the Tibetan area.

[4] Many Asian dust studies, including ground-based lidar observations [Murayama et al., 2001; Liu et al., 2002; Sugimoto et al., 2003], have focused on the late winter and spring due to observed long-range dust transport. There have been very few studies analyzing the specific signatures of summer and fall dust storms over the Tibetan Plateau. The recently launched CALIPSO satellite provides a wealth of actively sensed data over the region and provides an outstanding opportunity for studying Tibetan dust storms and their potential climatic effects. Unlike the previous generation of space-based remote sensing instruments, CALIPSO can observe aerosols over bright surfaces and beneath thin clouds as well as in clear sky conditions [Winker et al., 2006; Liu et al., 2004; Vaughan et al., 2004]. This study investigates Tibetan dust characteristics and physical properties using CALIPSO data. The origins of Tibetan dust storms are also examined using the HYbrid Single-Particle Lagrangian Integrated Trajectory (HYSPLIT) model [Draxler, 2006; Escudero et al., 2006] (http://www.arl.noaa.gov/ready/hysplit4.html).

2. Data

[5] The Cloud-Aerosol Lidar with Orthogonal Polarization (CALIOP) is the primary instrument on the CALIPSO satellite. CALIOP is designed to acquire vertical profiles of elastic backscatter at two wavelengths (532 nm and 1064 nm) from a near nadir-viewing geometry during both day and night phases of the orbit. In addition to total backscatter at the two wavelengths, CALIOP also provides profiles of linear depolarization at 532 nm. The depolarization measurements enable the discrimination between ice and water clouds, and the identification of non-spherical aerosol particles. CALIOP measurements taken from June through September 2006 over the Tibetan area (25–45°N, 75–100°E) were obtained to calculate the volume depolarization ratio and volume color ratio profiles. Note that the depolarization ratio and the color ratio are for total scattering, which is the combination of particulate and molecular scattering.

[6] Aura OMI (Ozone Monitoring Instrument) AAI (Absorbing Aerosol Index) data are also used in this paper. The AAI indicates the presence of ultraviolet (UV)-absorbing aerosols in the Earth's atmosphere, and is derived from a residual of the measured UV reflectance [Herman et al., 1997; Torres et al., 1998; de Graaf et al., 2005]. The AAI has been used for a long time to remotely sense UV-absorbing aerosols, such as desert dust [e.g., Moulin and Chiapello, 2004].

3. Results

[7] A typical example of the vertical distribution of a summer dust plume over the Tibetan plateau is shown in Figure 1. On 26 July, a moderate wind and dust storm, accompanied by localized severe dust storms, developed in and extended southward from North Xinjiang and the Tarim Basin. Under the influence of this storm, a wind-blown sand and/or dust cloud persisted over northern Qinghai and Tibet through 1 August. The CALIOP orbit-altitude cross section of the 532-nm total attenuated backscatter for 27 July 2006 at 2000 UTC in Figure 1a shows that a dust layer developed over the northern slope of the Tibetan Plateau and extended from ground level to a height of 5–9 km above mean sea level (MSL). The mineral dust layer had high values of backscatter indicating that the layer was thick. Its depolarization ratio was high because it was primarily composed of largely non-spherical particles. Figures 1b and 1c show the vertical profiles of backscatter intensity and depolarization ratio at 39.23°N, 88.93°E (left vertical line in Figure 1a) and at 37.89°N, 88.52°E (right vertical line in Figure 1a), respectively. The vertical profiles of the depolarization ratio clearly show the vertical structures of the dust layers over the Taklamakan desert (Figure 1b) and the northern slope of the Tibetan Plateau (Figure 1c). The depolarization ratio of 20–30% indicates the non-sphericity of the particles, which are assumed to be irregularly shaped dust.

Figure 1.

(a) The altitude-orbit cross-section of total attenuated backscattering intensity over Taklamkan-Tibet Plateau. (b) The vertical profiles of total 532 nm attenuated backscattering intensity (black curve) and depolarization ratio (green curve) about 20 GMT on 27 July 2006 at 39.23°N, 88.93°E. (c) Same as in Figure 1b but for 37.89°N, 88.52°E.

[8] The vertical distribution of dust plumes is one of the critical parameters in the assessment of dust radiative forcing [Claquin et al., 1998]. An analysis of observations by Minnis and Cox [1978] and a model study by Carlson and Benjamin [1980] showed that an elevated Saharan dust layer could change the atmospheric heating rate dramatically. Liao and Seinfeld [1998] claimed that clear sky long-wave radiative forcing and cloudy sky top-of-atmosphere (TOA) short-wave radiative forcing are very sensitive to the altitude of the dust layer. Meloni et al. [2005] found that SW aerosol radiative forcing at the TOA has a strong dependence on aerosol vertical profiles. One of the advantages of the CALIOP is that it provides a direct measure of the vertical structure of dust plumes. Figure 1 shows that the dust layer extends from 4 to 6.5 km over both the Taklamakan desert (Figure 1b) and the Tibetan Plateau (Figure 1c).

[9] Figure 2 shows the spatial distribution of the AAI on 28 July as derived from AURA satellite measurements that were taken about 12 hours later than the CALIPSO data in Figure 1. It is a semi-quantitative index of the columnar absorption by aerosols at 0.340 μm. The signal is derived from the absorption of the upwelling Rayleigh scattering from the lower strata of the atmosphere [Herman et al., 1997]. It can be seen in Figure 2 that the large AAI center is in the area surrounding the Taklamakan desert in Xinjiang. The Taklamakan desert area has a high frequency of dust storm occurrence, averaging more than 80 days each year. Dust aerosols from the Taklamakan Desert are entrained to an elevation of 5 km or higher and then transported over Tibet by the prevailing winds, which explains the structure seen in Figures 1 and 2. The AAI exceeds 0.5 over most of the Tibet area and is with values greater than 1.0 over northern Tibet. These large values indicate that the aerosols are highly absorptive.

Figure 2.

Aura OMI aerosol index over Taklamkan Desert and Tibet Plateau on 28 July 2006.

[10] To perform a statistical study of Tibetan dust plume optical properties, 10 night-time cases were selected (see Table 1). Figure 3 summarizes the composite frequency distributions of the volume depolarization ratio (Figure 3a, the ratio between the parallel component and the perpendicular component of the lidar backscatter) and the total volume color ratio (Figure 3b, the ratio between 1064 nm lidar backscatter and 532 nm lidar backscatter) as functions of altitude for these cases. As shown in Figure 3a, the depolarization ratio decreases significantly with increasing altitude. For lower layers at altitudes from 3 to 5 km, the depolarization ratio for 64% of the pixels exceeds 20%, is between 10 and 20% for 26% of the dust pixels, and is less than 10% for the remaining 10% of the dust pixels. The larger depolarization ratio indicates the presence of highly concentrated desert dust that is probably very irregular in shape. Note that the volume depolarization ratio is particle concentration dependent, that is, the higher the dust concentration, the greater the volume depolarization ratio (the closer to the particulate depolarization ratio). However, the presence of spherical aerosols can reduce the dust volume depolarization ratio. In the free troposphere, between 7 and 10 km, the depolarization ratios for 47% of the dust pixels are less than 10% and between 10 and 20% for 28% of the pixels, where the dust concentration is low relative to the molecular density. The features of depolarization ratios observed in the middle troposphere, between 5 and 7 km, fall between the values observed for the free and lower troposphere. The depolarization ratio frequency percentages were 20%, 33% and 47% for the 0–10%, 10–20% and >20% ranges, respectively. In comparison to the volume depolarization ratio, the distributions of volume color ratio with values ranging from 0.6 to 0.9 (Figure 3b) remain relatively unchanged vertically although data with low depolarization ratio values have been removed.

Figure 3.

Frequency distribution of (a) the depolarization ratio and (b) the color ratio as functions of altitude for the 10 selected cases.

Table 1. Summer Tibetan Dust Storm Cases Selected From June to September 2006
CaseDateStart Point of Backward TrajectoryGround Height at Start Point, m
1June 27, 200636.67°N, 91.25°E4611.6
2July 9, 200636.00°N, 85.00°E4979.0
3July 27, 200636.11°N, 87.99°E4995.6
4July 30, 200636.11°N, 80.26°E4297.1
5August 1, 200634.92°N, 83.01°E5239.8
6August 12, 200636.11°N, 87.97°E5006.7
7August 19, 200636.11°N, 86.43°E5040.1
8September 4, 200637.57°N, 86.62°E3516.8
9September 6, 200636.11°N, 89.48°E4914.2
10September 20, 200636.41°N, 86.46°E4938.7

[11] To investigate the dust aerosol origins, air mass trajectories were computed with the HYSPLIT model for the 10 cases listed in Table 1. Back trajectories with starting points, based on the CALIPSO observation, were computed for a 4-day period. The starting points from the back trajectory analyses (i.e., the end point of dust transport) are marked with stars in Figure 4. The horizontal trajectory curves show that the dust plumes observed over the Tibetan Plateau all originated from the Taklamakan Desert. However, the back trajectories show that the dust particles are not directly lofted to the Tibetan Plateau but that most transports occur around the anticyclonic pathway. The dust first moves eastward and then turns to the south around the edge of desert. After that the dust moves westward and accumulates over the northern slopes of the Tibetan Plateau where eventually it is lofted up over the plateau. This pathway may be related to the low thermal cyclone that occurs when dust storms are observed in the Taklamakan Desert.

Figure 4.

Four-day back trajectories of air parcels climbing upon the Tibet Plateau for the 10 cases listed in Table 1. The gray dots represent surface observation station.

4. Conclusions and Discussion

[12] This paper presents direct Tibetan dust aerosol measurements from CALIPSO observations during summer, a season that is typically inactive for the development of dust storms. The dust particles primarily originate from the nearby Taklamakan desert and accumulate over the northern slope of the Tibetan Plateau. Because surface stations are mainly located on the eastern Tibetan Plateau, no surface observations are available over the northwestern region due to high elevation and harsh climate. However, during summer most Tibetan dust plumes develop elsewhere and are transported over western Tibet and remain undetected from the surface. Thus, satellite remote sensing data are crucial for detecting the Tibetan dust plumes and for estimating the optical properties and radiative impacts of the particles. For example, CALIPSO detected approximately 48 Tibetan dust plumes from a total of 90 nighttime overpasses over Tibet for the period from 14 June to 30 September 2006. According to the CALIPSO observations, the frequency of occurrence of summer dust plumes over the region (25–45°N, 75–100°E) under study is about 53%, which is much higher than results obtained from surface observations. The total averaged dust events (floating-dust and blowing dust plus dust storm) observed from the surface stations (box region in Figure 4) is less than 10% for the 4-month period from June to September (X. Wang, personal communication, 2007). It is far less than the frequency detected by CALIPSO. Although the difference between CALIPSO and surface observations may be related to other factors, the CALIPSO measurements provide a wealth of previously unknown information. Of course, this study is only a first step in quantifying the effectiveness of CALISPO for identifying dust plumes over the Tibetan Plateau. Further research should be focused on a combination of CALIPSO measurements with other NASA A-Train satellite measurements. The NASA A-Train satellites can provide near-simultaneous measurements of aerosol optical and radiative properties, cloud and aerosol vertical structure, cloud properties, and water vapor profiles. By combining TOA fluxes from the Clouds and Earth's Radiant Energy System (CERES) scanners and aerosol/cloud properties retrieved from the Moderate Resolution Imaging Spectroradiometer on Aqua with the vertical distributions of aerosols and clouds from CALIPSO, it should be possible to reliably determine dust aerosol radiative forcing over this remote area where heavy dust loadings occur much more frequently than expected.

Acknowledgments

[13] This research is supported by National Basic Research Program of China (2006CB400501) and NASA Science Mission through the CERES Project. The CALIPSO data were obtained from the NASA Langley Research Center Atmospheric Sciences Data Center. The OMI AAI image and data used in this study were acquired using the GES-DISC Interactive Online Visualization and Analysis Infrastructure as part of the NASA's Goddard Earth Sciences Data and Information Services Center. The authors also gratefully acknowledge the NOAA Air Resources Laboratory for the provision of the HYSPLIT transport and dispersion model and/or READY website (http://www.arl.noaa.gov/ready.html) used in this publication.

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