Our understanding of the global dust cycle is limited by a dearth of information about dust sources, especially small-scale features which could account for a large fraction of global emissions. Here we present a global-scale high-resolution (0.1°) mapping of sources based on Moderate Resolution Imaging Spectroradiometer (MODIS) Deep Blue estimates of dust optical depth in conjunction with other data sets including land use. We ascribe dust sources to natural and anthropogenic (primarily agricultural) origins, calculate their respective contributions to emissions, and extensively compare these products against literature. Natural dust sources globally account for 75% of emissions; anthropogenic sources account for 25%. North Africa accounts for 55% of global dust emissions with only 8% being anthropogenic, mostly from the Sahel. Elsewhere, anthropogenic dust emissions can be much higher (75% in Australia). Hydrologic dust sources (e.g., ephemeral water bodies) account for 31% worldwide; 15% of them are natural while 85% are anthropogenic. Globally, 20% of emissions are from vegetated surfaces, primarily desert shrublands and agricultural lands. Since anthropogenic dust sources are associated with land use and ephemeral water bodies, both in turn linked to the hydrological cycle, their emissions are affected by climate variability. Such changes in dust emissions can impact climate, air quality, and human health. Improved dust emission estimates will require a better mapping of threshold wind velocities, vegetation dynamics, and surface conditions (soil moisture and land use) especially in the sensitive regions identified here, as well as improved ability to address small-scale convective processes producing dust via cold pool (haboob) events frequent in monsoon regimes.
 Mineral dust affects climate by absorbing and scattering solar and terrestrial radiation as well as by modifying cloud properties [Forster et al., 2007]. In addition, dust mediates carbon uptake by providing iron, a limiting nutrient in many ocean regions [Jickells et al., 2005], and phosphorous to land surfaces (e.g., the Amazon forest [Swap et al., 1992]). As one of the most abundant aerosols in the atmosphere, dust has also important implications regarding air quality [Prospero, 1999]. In order to estimate the impacts of dust on climate and air quality, the factors controlling dust emissions must be identified and quantified. This objective has been the focus of numerous studies based on field campaigns, laboratory measurements, satellite data, and model simulations. Still, there are large uncertainties regarding the impact of anthropogenic activities on modulating dust emission directly, e.g., by disturbing soils, removing vegetation cover, or desiccating water bodies, and indirectly, by changing climate and the hydrological cycle. In addition, most of the existing studies focus on local or regional scale and rarely quantify their global impact. Present estimates of the anthropogenic contribution to global dust emission range from less than 10% [Tegen et al., 2004] to a maximum of 50% [Mahowald and Luo, 2003]. Such large uncertainty may be attributed in large part to the lack of global detailed characterization of dust sources.
 The objective of the present study is to develop a new satellite product that has adequate resolution to detect and attribute natural and anthropogenic dust sources and to use this product to assess anthropogenic and hydrologic impacts on dust emission at the global scale. These results are evaluated against a wide range of observational evidence.
 Satellite data analysis by Prospero et al.  showed that most major dust sources are located in arid regions in topographic depressions where deep alluvial deposits have formed by intermittent flooding through the Quaternary and into the Holocene. Although the sources are located in arid regions, the action of water is evident from the presence of ephemeral streams, rivers, lakes, and playas (ephemeral or desiccated lakes which contain deposits of clay, silt, and salts). In some of these depressions, the layer of alluvium is sufficiently deep to sustain dust emission without further replenishing, but others are regularly flooded, thereby forming new sediment deposits. Although within a basin ephemeral lakes provide ideal conditions for wind erosion, ephemeral riverbeds (e.g., wadis or arroyos) also have the potential to be active dust sources. Most recent field studies of dust sources have focused on ephemeral lakes, for example, Owens Lake [Gillette et al., 1997] and Franklin Lake [Reynolds et al., 2007] in the Great Basin of the USA, the Bodélé depression as characterized during the Bodélé Dust Experiment (BoDEx) field campaign [Washington et al., 2006], the Etosha Pan in Namibia [Bryant, 2003], the Chotts of Tunisia and Algeria [Mahowald et al., 2003], the Makgadikgadi pans in Botswana [Bryant et al., 2007], the Lake Eyre basin of Australia [Bullard et al., 2008], the Mar Chiquita of Argentina [Troin et al., 2010], and Lake Ebinur of northwest China [Abuduwaili et al., 2008]. They all show that dust emission depends on the interplay of characteristics of sediments, soil moisture, groundwater, and vegetation. Some show an increase of dust emission after inundations, which provide fresh deposits of fine sediments. But Mahowald et al. noted that the role of ephemeral lakes is unclear on a regional scale and even less clear at the global scale. The main reason cited by the authors is the difficulty in interpreting coarse-resolution satellite data.
 Source identification is even more difficult for small-scale sources (the “hot spots” defined byGillette ) such as floodplains, alluvial fans, rivers, and wadis. Using a global model, Zender et al.  studied the importance of sediment availability and erodibility in reproducing dust distribution and deposition. They concluded that although evidence suggests that these were quite important, they could not support their conclusions with direct observations because of limited resolution over dust sources. These studies are indicative of the growing recognition of the great spatial and temporal diversity of dust source environments. Thus, in order to understand the global dust cycle it is critical to quantify the relative importance of the different types of sources and the factors that affect emissions, as noted by Okin et al.  and Bullard et al. .
 Even more uncertain is the impact of human activities on dust mobilization. Mahowald et al. , by constraining a dust model with observations, estimate that global dust loads have doubled in the twentieth century due to anthropogenic activities. A review by Gill  documents many examples in numerous nations of the effects of anthropogenic land disturbance and the desiccation of playas. Neff et al.  link the expansion of livestock grazing in the early twentieth century with a 500% increase of dust deposition in the western United States. Agricultural practices have long been recognized as a key factor in producing the “Dust Bowl” in the 1930s [Orlove, 2005; Cook et al., 2009]. Cropland and rangelands are still the main sources of dust in the southern high plains of North America [Stout, 2001; Lee et al., 2012]. Since the end of the nineteenth century, there have been reports of new dust sources created by water diversion for irrigation, Owens Lake [Gillette, 1999], the Aral Sea [Micklin, 2007], and Lake Ebinur [Abuduwaili et al., 2008] being examples. On the other hand, restoration and mitigation of degraded land have reduced dust activity from Lake Texcoco, Kara-Bogaz Gol, and the Konya Basin [Gill, 1996]. In China, Ma et al.  have shown that over the last half century 243 lakes have vanished, while 60 new lakes appeared, mostly due to human influence and global warming.
 Projections of atmospheric dust in response to climate change have been simulated using different general circulation models [e.g., Tegen et al., 2004; Mahowald et al., 2006]. The results of these simulations differ substantially not only in their projections but also in the present-day dust distributions.Huneeus et al. , retrospectively comparing the results of 15 dust models for the year 2000, found very large disparities among models, especially in their emissions. These model studies emphasized the need of satellite observations to better characterize dust loads over source areas.
 Satellite instruments are the most useful tool to locate dust sources as they provide near-daily global observations.Ginoux et al. discussed various satellite products, including Moderate Resolution Imaging Spectroradiometer Deep Blue (MODIS DB) Level 2 (henceforth M-DB2) aerosol products, and demonstrated their use to identify dust sources in West Africa. The advantages of M-DB2 products as retrieved byHsu et al. are their high resolution (∼10 km), daily near-global coverage, and spectral information (aerosol products at multiple wavelengths). A limitation of these products is that they can only be retrieved over bright surfaces in the visible, a restriction that consequently excludes forests and ocean surfaces which, in any event, are not significant dust sources. However, we are aware of at least two regions where M-DB2 cannot retrieve dust sources. One is in Iceland, where dust sources identified byProspero et al. are associated with active glacial outwash plains, which are too dark to be retrieved from M-DB2. The other is in Alaska, where dust plumes are emitted within the solar terminator, which necessitates special treatment of satellite backscatter radiances to effectively retrieve dust sources [Crusius et al., 2011]. Another limitation of polar orbiting satellites is the lack of continuous measurements as they measure backscattered radiances of an area only once a day. Ginoux and Torres  have cautioned that by using polar orbiting satellite products, one might miss sources that become active after satellite overpass. This has been clearly shown with some case studies based on geostationary satellite data [Schepanski et al., 2007]. However, Smirnov et al. , using multiple years of Sun photometer data, show that the variability of aerosol optical depth in dusty environments is typically less than 10% over the course of a daylight day.
 Here we extend the work of Ginoux et al.  to the global scale. In addition, we assess our results through comparison with other data sets and estimate the contribution of each source type to dust emissions. In section 2, we provide a summary of our methodology. We briefly describe in section 3the gridded M-DB2 data. Insection 4, we first present the method to derive dust optical depth (DOD) from M-DB2 products and compare it to Aerosol Robotic Network (AERONET) Sun photometer data. We then analyze the spatial and frequency-of-occurrence (FoO) distributions of DOD. Insection 5, the detection of dust sources is described and the resulting distribution is compared with inventories from other satellite instruments: the Total Ozone Mapping Spectrometer (TOMS) and the Ozone Mapping Instrument (OMI). Next we classify the sources according to land use and hydrologic origin, and we examine in detail dust sources in different continental regions. In section 6, we calculate the contribution of dust emissions from bare ground, vegetated areas, ephemeral water bodies, and land use. In section 7 we discuss the implications of our results on climate, air quality, and health. Finally, we present our conclusions in section 8.
 For clarity, we summarize the five main steps of our methodology.
Dust optical depth.After mapping daily M-DB2 aerosol products on a Cartesian 0.1° latitude-longitude grid, DOD is derived from the aerosol optical depth (AOD) using criteria based on size distribution and optical properties. The results of this technique are tested against AERONET Sun photometer data.
Background DOD. The frequency distribution is analyzed and used to determine a minimum DODthresh that could be ascribed to background aerosols.
Source detection. The FoO distribution of DOD > DODthresh is used to identify active dust sources, and the results are compared to similar analyses derived from TOMS and OMI satellite data.
Source attribution. Source areas are attributed to an anthropogenic or hydrological origin based on, respectively, the degree of land use and the presence of ephemeral water bodies.
Source emissions.The contributions of anthropogenic and hydrological sources to dust emissions are calculated using wind speed from a high-resolution model.
3. GRIDDED MODIS DEEP BLUE DATA
 The M-DB2 algorithm employs radiances from the blue channels of MODIS instruments. At these wavelengths the surface reflectance is very low so that the presence of aerosol is detected by an increase of total reflectance and enhanced spectral contrast [Hsu et al., 2004, 2006]. The values of AOD and single scattering albedo (ω) at 412, 470, 550, and 670 nm and the Angstrom exponent (α) between 412 and 470 nm are retrieved at the pixel level over bright surfaces (reflectance at 550 nm greater than 0.15) and then averaged over a 10 km × 10 km grid. The data are aggregated into granules which comprise the level 2 data. Ginoux et al. used collection 5.0 level 2 products from MODIS on the Aqua platform. For the present study, we use data from the same instrument but with the improved collection 5.1 data from 2003 to 2009. The improvements include updated characterizations of the surface bidirectional reflectance distribution function and cloud screening techniques. All aerosol products are interpolated on a regular 0.1° latitude-longitude grid using the algorithm described byGinoux et al. .
 The number of M-DB2 retrieval per 0.1° × 0.1° grid cell and per season (averaged from 2003 to 2009) is shown inFigure 1. Some regions yield no data because either their surface reflectance in the visible is below 0.15 (oceans and forests) or they were not considered in this study (Central America and Southeast Asia). Other regions yield reduced data due to the presence of clouds. These are mostly areas influenced by the monsoon (for example, in India) or located along the Intertropical Convergence Zone (ITCZ). Over arid and semiarid regions the number of valid retrievals is on average higher than 30 days per season, i.e., more than 30%.
4. MODIS DUST OPTICAL DEPTH
 After all the data have been gridded, a screening method is applied to extract scenes of AOD dominated by dust. The screening protocol applies three conditions that are based on size distribution, absorption of solar radiation in the green (550 nm), and the contrast of absorption between the red (670 nm) and deep blue (412 nm) channels.
 Dust size distributions are characterized by the presence of a prominent coarse mode (particle size greater than 1 μm radius) in contrast to urban and biomass burning aerosols, which yield abundant fine-mode aerosols (particle size less than 1μm) [Dubovik et al., 2002]. Gravitational settling efficiently removes large particles, and consequently, the dust size distribution shifts to smaller radii with increasing transport time. Eck et al.  show that the dominance of one mode over the other can be measured with the Angstrom wavelength exponent α. The α values range from −0.5 to 0.5 in dusty environments; they are greater than 0.5 in polluted regions. Schepanski et al.  have imposed α< 0.6 to detect dust using the infrared channels of the Spinning Enhanced Visible and Infrared Imager instrument on the Meteosat Second Generation satellite. However, we would like to apply a more stringent criterion so as to screen out all scenes with any significant amount of fine-mode particles, either from other aerosol types or aged dust. Many measurements in dusty environments yield negativeα during dust outbreaks and near dust sources: from −0.2 to 0.04 (during three flights) in Niger [Osborne et al., 2008], −0.06 (three events) in Delhi [Singh et al., 2005], −0.5 (one event) in Spain [Cachorro et al., 2000], less than 0 at Birdsville (many events mostly in summer but also in fall) in the Lake Eyre basin [Radhi et al., 2010], and −0.24 (typical during dust storms) in Tengger Desert in northern China [Xin et al., 2005]. Cheng et al.  reported negative values 11.4% and 6.7% of the time over 5 years of measurements near Chinese dust sources at Dunhuang and Yulin, respectively.
Schuster et al.  show that for a monomodal distribution of coarse particles, α is negative for effective radius greater than 1 μm. Typically, for coarse-mode dust the effective radius is about 2μm [Dubovik et al., 2002; Osborne et al., 2008]. Based on these various observations we impose as our first dust criterion that α < 0.
 Although M-DB2 products are retrieved only over bright surfaces in the visible (to not be mistaken with brightness in the deep blue, which is always small), thereby excluding oceans, there may be scenes in coastal regions where sea salt concentrations are high. Because sea salt has a significant amount of coarse-mode particles, lowα values could result. To avoid this situation, we require that the single scattering albedo ω at 412 nm is less than 0.95. For scattering aerosols such as sea salt ω is near 1. This second criterion efficiently eliminates sea salt–dominated scenes. We should note that some dust sources contain a large percentage of salt, for example, the Aral Sea [Rudich et al., 2002]. Internal mixing of dust and salt will affect the optical characteristics of pure dust, but it is not clear how it could affect our results. The mixture will still absorb shortwave radiation, although more weakly. In the following sections, we will show that our scheme successfully detects dust near salty sources such as the Aral Sea, Owens Lake, and Great Salt Lake, among others.
 Another specific optical property of dust is the sharp increase of absorption from red to deep blue. This translates into a positive spectral variation of ω with wavelength. Internal mixing with nonabsorbing sea salt should theoretically not change the sign of dust spectral variation of absorption. This is also true for nonabsorbing sulfate aerosols. The third criterion requires a positive difference of ω between 412 and 670 nm (ω670 − ω412 > 0). Using these three criteria based on the physical and optical properties of aerosol, we extract the global distribution of daily DOD from the retrieved AOD over the period 1 January 2003 to 31 December 2009.
4.1. Comparison With AERONET
 To evaluate our screening method using M-DB2 products, we apply it to the direct measurements of AOD made in the AERONET Sun photometer network. AERONET is a federated worldwide network of Sun photometers that are monitored and maintained at NASA Goddard Space Flight Center [Holben et al., 1998]. We use aerosol optical depth and the Angstrom exponent (440–670 nm) level 2 data, which are cloud screened and quality assured; these are available at http://aeronet.gsfc.nasa.gov. From all measurements collected between 2003 and 2009 and from all sites, we extract AERONET data between 12:00 PM and 3:00 PM local time. This provides a 3 h window centered at 1:30 PM, the local passing time of the MODIS instrument on Aqua. We only use M-DB2data within a 30 km window centered on the AERONET site. The spectral values of single scattering albedo are also retrieved by inversion of almucantar measurements [Dubovik and King, 2000]. The almucantar measurements are performed by keeping the same solar zenith angle while varying the azimuthal angle of the Sun photometer over 360°. However, the level 2 quality assured inversion products are computed only for AOD greater than 0.4. This condition would severely limit the number of collocated measurements. Therefore, the only dust criterion that we require of the AERONET data is that α < 0.
Figure 2(top) shows the comparison between the spatially and temporally collocated mean AOD (550 nm) measured by AERONET and retrieved by M-DB2 algorithm, as well as, inFigure 2(bottom), the mean DOD (550 nm) extracted from AERONET and M-DB2 data. We found 195 and 13 AERONET sites with collocated measurements of AOD and DOD, respectively. There is a significant correlation between AERONET and M-DB2 for AOD as well as DOD. The root-mean-square differences are 0.11 and 0.26, while the mean absolute differences are 0.07 and 0.24 for AOD and DOD, respectively. Although AOD sites are widespread and include polluted regions with aerosol dominated by fine-mode particles, the screening method selects only sites known to lie nearby to dust sources. The largest biases in AOD and DOD are in California and Australia. In Africa, M-DB2 AOD is slightly overestimated while DOD is systematically underestimated by 25%–50%. The largest DOD value inFigure 2 corresponds to the Kanpur (India) site.
Table 1 gives the mean AOD and DOD values and the number of days with collocated measurements at the 13 AERONET sites. While there are hundreds of AOD measurements per site, the number of days with collocated measurements satisfying DOD conditions is dramatically reduced, ranging from 104 days in Agoufou (Mali) to a minimum of 8 days in Rogers Lake (California). Table 1shows that at all sites the mean DOD is significantly larger than the mean AOD, with the highest mean DOD (1.5 for M-DB2 and 1.4 for AERONET) at Kanpur (India). The lowest DOD values are observed at the Tinga Tingana and Birdsville sites, both of which are in the Lake Eyre Basin of Australia. The annual AERONET DOD is 0.16 for both sites; M-DB2 values are higher, 0.34 for Birdsville and 0.19 for Tinga Tingana. These data show, as expected, that the imposed conditionα< 0 effectively serves to identify dust events and to discriminate against air parcels containing fine-mode pollutants.
Table TABLE 1.. Collocated Mean Aerosol (AOD) and Dust (DOD) Optical Depth at 550 nm Measured by AERONET and Retrieved From M-DB2, at 13 AERONET Sitesa
The number of days with collocated measurements (N) of AOD and DOD are provided for each site. IER, Institut d'Economie Rurale.
4.2. Seasonal Distribution
 Comparisons between monthly mean and standard deviation of AOD from AERONET and M-DB2 and DOD from M-DB2, calculated from measurements between 2003 and 2009, are shown inFigure 3. For this comparison, all M-DB2 data are selected within a 30 km window centered on the location of the AERONET sites but without restricting local passing time between 12:00 PM and 3:00 PM. The values inFigure 3are calculated by averaging all valid AERONET level 2 measurements and M-DB2 retrievals. M-DB2 monthly AODs are within the standard deviation of AERONET data in Africa, Arabian Peninsula, and India but largely overestimated in California, Australia, and Israel. These discrepancies were already apparent inFigure 2. Most sites in Africa are located within or approximate to the Sahel, one of the most active dust sources in North Africa (Dakar, Agoufou, Cinzana, Banizoumbou, and Soroa). The Cape Verde Islands site is located off the west coast of North Africa, under the path of much of the dust that emerges from North Africa. Tamanrasset is a mountain site (1377 m above sea level) located in the Sahara. At the Tamanrasset site, there is a distinct peak of M-DB2 DOD in June, in agreement with the measurements taken in 2006 byCuesta et al. at that location. The seasonal cycle at the Sahel sites differs from Tamanrasset in that dust is a significant contributor to AOD from January to July. The M-DB2 seasonality is supported by measurements made byRajot et al.  at Banizoumbou during the African Monsoon Multidisciplinary Analysis field campaign in 2006.
 In Solar Village (Arabian Peninsula), there is a pronounced maximum of M-DB2 DOD in April-May; dust activity weakens rapidly in summer, reaching a minimum in winter, in accordance with observations ofSabbah and Hassan . At Kanpur (India), large amounts of dust are observed during the premonsoon season with M-DB2 DOD reaching 0.8 in May-June; in contrast, M-DB2 DOD shows no dust during the other seasons. The greatest discrepancies are seen at Sede Boker (Israel), Birdsville (Australia), and Rogers Lake (California), where M-DB2 AOD is largely overestimated.
 The 7 year mean seasonal variation of M-DB2 AOD and DOD at 550 nm is shown inFigure 4. DOD distribution is plotted for all values of DOD greater than 0.1; elsewhere, AOD is plotted so that the relative distribution is made visible. The Northern Hemisphere is clearly much more dusty than the Southern Hemisphere both in terms of the absolute values of DOD and the spatial coverage. The same is true for AOD. In both hemispheres, fall is the season with the lowest DOD values: September, October, and November (SON) in the Northern Hemisphere and March, April, and May (MAM) in the Southern Hemisphere.
 There are many regions with DOD > 0.1 all year long. The most widespread dust activity is seen in North Africa, especially within the Sahel, a region that is broadly defined in terms of rainfall as the zone lying between the 100 and 500 mm isohyets [National Research Council, 1983], which in West Africa lies roughly between 14°N to 20°N. This region encompasses three phytogeographical divisions: the northerly Sahelo-Saharan zone (grass steppe), between the 100 and 200 mm isohyets; the Sahel proper (tree steppe), between the 200 and 400 mm isohyets; and the southerly Sudano-Sahelian borderlands (shrub savanna), extending to the 500 mm isohyet. The Sahel has been the focus of much interest because of the great increase in dust activity that occurred following the onset of prolonged drought in the early 1970s [Prospero and Lamb, 2003].
 In West Africa, DOD is consistently higher in the Sahel (including Senegal, Mauritania, Mali, Niger, and Chad) than in the Sahara, although most studies of dust activity have focused on major sources in the Sahara [Prospero et al., 2002; Schepanski et al., 2007]. However, Maurer et al.  pointed out that the Sahel region is one of the Earth's most wind erosion–prone zones because these soils, which largely overlie sand sheets, are intensively developed for agriculture and thus become vulnerable to wind erosion. The region is influenced by the dry Harmattan winds from the north and the monsoon flow from the Gulf of Guinea. These two flows converge at the surface along the Intertropical Discontinuity (ITD) and in the free troposphere along the ITCZ. There does not seem to be any seasonal variation of these hot spots in Figure 4 despite the fact that the ITD shifts from 5°N in winter to around 18°N in summer [Bou Karam et al., 2008]. This quasi-permanent maximum DOD in the Sahel may be a result of the combination of both emissions from local sources and transport from other upwind regions.Klose et al.  analyzed weather reports from 1983 to 2008 and found the existence of a zone of frequent dust events and high dust concentration in the Sahel. The dust events are reported as mostly dust in suspension, which suggests that transport from the Sahara to the Sahel is more important than local emissions. Nonetheless, weak dust sources in the Sahel may be significant as pointed out by the modeling study of Guelle et al. .
 It is interesting to note that most models do not produce a large amount of emissions from the Sahel. Among the 15 global dust models analyzed by Huneeus et al. , few reproduce the most southward displacement of the Saharan dust cloud in winter. This disparity may be related to the resolution of these models. Indeed, Bou Karam et al. observed haboob-type dust events during the passage of a density current that originated from a mesoscale convective system situated on the leading edge of the monsoon flow. Using a 20 km resolution model,Bou Karam et al.  suggested that emissions driven by strong surface winds associated with these density currents may contribute significantly to the total dust load over West and North Africa. However, using a model with similar resolution (25 km), Haustein et al. had difficulty simulating an observed dust storm in the Sahel associated with intense moist convection. Using a higher-resolution (7 km) regional model,Tegen et al.  could reproduce a heavy dust plume over the Bodélé depression, although the model underestimates wind speed over the region. Similar resolution will be necessary to confirm the importance of downdrafts from convective storms over the Sahel, as well as other monsoon regions.
 Some of the most intense hot spots are in the northern part of the Sahel. The best example is the much studied Bodélé depression (17°N, 18°E, 170 m) in Chad [Koren et al., 2006; Washington et al., 2006; Todd et al., 2007] which yields an annual mean DOD value greater than 0.75. This high value is in agreement with the mean AOD = 1.1 retrieved from Multiangle Imaging Spectroradiometer (MISR) and reported by Koren et al. . One of the few studies measuring DOD in this region [Osborne et al., 2008] reported values up to 0.8 during dust events over Niger.
 Over North Africa, there are regions where DOD < 0.1 and AOD > 0.25. They are mostly located in the Sahara where sulfate emitted by fossil fuel burning and transported from Europe [Lelieveld et al., 2002] may contribute significantly to AOD. Also along the southernmost areas of the Sahel, we expect carbonaceous aerosols from biomass burning to contribute significantly to AOD, especially in winter [Crutzen and Andreae, 1990].
 Over the Middle East, the regions with the highest and most widespread FoOs of DOD > 0.1 are in Mesopotamia and along the Persian Gulf in MAM. There are also a few local spots in the coastal regions of Yemen and Oman with mean DOD greater than 0.25, mostly in MAM and June, July, and August (JJA). In central Asia, DOD > 0.1 is found over the east Aral Sea, the southeast coastal region of the Caspian Sea, the eastern parts of Uzbekistan and Turkmenistan, and the southwest corner of Afghanistan, all of which are known sites of highly active dust sources.
 In Figure 4, India is characterized by a strong seasonal and latitudinal variation of DOD. The peak period for dust is March, April, and May (premonsoon), and the weakest period is in September, October, and November (postmonsoon). During the premonsoon period, DOD is >0.5 over the Indo-Gangetic basin. During the monsoon period (June, July, and August), the number of retrievals is too low (cf.Figure 1) to make any conclusion about DOD or AOD in Figure 4. But after the monsoon period and in winter, the region appears free of a significant amount of dust.
 Recently, Dey and Di Girolamo  derived a climatology of nonspherical aerosol optical depth over India using MISR data. For the most part, the seasonal variation and latitudinal gradients are similar, but the absolute values of DOD are more than a factor of 5 lower in their study. As shown above (Figure 3), we overestimate AOD by a factor of 2 in Kanpur in May and June, while in their study they underestimate AERONET AOD by a factor of 2 at Kanpur.
 Data are only consistently obtained in NW and NE China where the AOD and DOD distributions show a significant seasonal and spatial variation. DOD coverage and amplitude are at a maximum in spring, in agreement with previous studies [Sun et al., 2001; Wang et al., 2004]. DOD makes a significant contribution to total AOD only during this most active dust season and only in the NW region. It is notable that in NE China, AOD dominates DOD in spring, despite the fact that intense, large-scale dust events are common throughout the region. This is most likely related to the large contribution of fine-pollutant aerosol to optical depth and the low frequency of dust events, as discussed in the next section. The intense and widespread dust activity seen in NW China in MAM is mostly associated with basins that have been previously identified: Tarim, Qaidam, Junggar, and Turpan [Prospero et al., 2002]. Over these regions, the seasonal mean DOD varies between 0.1 and 0.5 in MAM but drops below 0.1 in most areas during the other seasons. In JJA, some areas of the Tarim and Qaidam basins are still dusty; in the Tarim, there are two strong sources (DOD maxima > 0.5), one in the NE and one in the SW of the basin. Ge et al. showed that M-DB2 retrievals agree relatively well with ground-based data during dust events in northwest China. They observed AOD varying from 0.07 to 2.5 during dust events, with M-DB2 performance improving with increasing AOD.Christopher and Wang  showed similar daily variations (from 0.2 to 1.5) during dust events over Dunhuang (40.1°N, 94.4°E), which is located near the Tarim Basin and Gobi dust sources.
 In North America, DOD > 0.1 are seen around Baja California and the southern high plains in Texas. Some hot spots with DOD > 0.25 are observed in MAM over the Salton Basin of southern California, the Gila Valley in southwest Arizona, along the Pecos River of southwest Texas, the Vizcano Desert of the central part of the Baja California, and the Playa de San Nicolas in the southern part of the Sonoran Desert in Mexico. In Europe, the only two regions with DOD > 0.1 are located in Spain's Meseta Central and Anatolia in Turkey, but only in JJA.
 In the Southern Hemisphere, Australia is the only continent that yields substantial areas with DOD > 0.1; dust activity is greatest in SON, Austral spring. Over some ephemeral lakes within the Lake Eyre Basin, DOD is higher than 0.25 from September to February. But, as seen in Figure 3, M-DB2 AOD and DOD are largely overestimated in Australia. The other regions in the Southern Hemisphere with DOD > 0.1 are mostly areas within deserts, e.g., the Namib (Namibia), Kalahari (Namibia), Atacama (Chile), and Sechura (Peru) Deserts.
4.3. Frequency Distribution
 In this section, we analyze the FoO of optical depth by region and season with the objective of developing a procedure to identify major dust storm days based on the relative frequency of magnitude of DOD and AOD. To this end we divided the continents into seven regions defined in Table 2. The number of samples per region is large and varies between 105 to 107 depending on the season. Table 3 provides the percent cumulative frequency for three values of optical depths (0.25, 0.5, and 1) and for each region and season.
Table TABLE 2.. Domain of the Continental Regions Considered in This Study
Table TABLE 3.. Cumulative Frequency Distribution (Expressed in Percentage) of M-DB2 DOD and AOD (in Parentheses) ≤0.25, 0.5, and 1 Over Five Continental Regions for Each Seasona
DJF, December, January, and February; MAM, March, April, and May; JJA, June, July, and August; SON, September, October, and November.
 In all regions, for all seasons, and for all three optical depth values in Table 3, the cumulative frequencies of AOD are much greater than those of DOD. The frequency of AOD > 0.25 is generally lower than 50%, except during MAM in west and central Asia, while DOD is most frequently greater than 0.25 for all regions. Therefore, a DOD threshold DODthresh = 0.2 is selected to distinguish dust events from background aerosols.
 The global distribution of the number of days DOD > 0.2 for each season is shown in Figure 5. The global distribution of dust event days with DOD > 0.2 shown in Figure 5is broadly similar to that of the mean M-DB2 AOD and DOD shown inFigure 4. The most widespread occurrence and the highest frequencies are seen in North Africa. Within the Sahel, events with DOD > 0.2 occur at least seven times per season and more than 75% of the time in certain areas (e.g., Mauritania, Niger, and the Bodélé depression). Engelstaedter et al.  used visibility data to develop a global map of annual dust storm frequency which shows distributions in the Sahel that are remarkably similar to those in Figure 5, taking into consideration that our results are based on seasons. Other areas with frequent events are Mesopotamia in summer, the Iranian coastal region all seasons, eastern Uzbekistan and Turkmenistan in summer, and the Indo-Gangetic basin during premonsoon season. On the other hand, the number of dust events in Inner Mongolia and Mongolia appears to be low. Ground-based visibility data appear to support this low frequency of dust outbreaks in China. Using visibility data from 1988 to 2004 over the entire east Asian continent,Kurosaki and Mikami  showed that the frequency of dust outbreaks in China is greater than 4% (corresponding to 4 days per season in Figure 5) only in the Tarim Basin, the Gobi Desert, and the Loess Plateau. These are the regions in Figure 5where M-DB2 frequencies are greater than 7 days in MAM and JJA.
 In North America, the highest frequency of dust events is found in the southwestern U.S. and northern Mexico. Along the border between the U.S. and northern Mexico, events with DOD > 0.2 appear as frequently as 30% of the time in MAM. This is in agreement with the long-term record of visibility data at El Paso (Texas), where there is high frequency of blowing dust in spring [Novlan et al., 2007]. There is also considerable dust activity in the western great plains in MAM.
5. MODIS DUST SOURCES
 After emission, dust concentration decreases by gravitational settling, dry deposition at the surface, and wet removal in and below clouds [Ginoux et al., 2001]. As long as the sources are active, DOD retrieved from instantaneous satellite measurement will be at a maximum over the sources. But dust emission is generally episodic, and subsequently, the maximum DOD will move with the plume. Nonetheless, as meteorological conditions change from day to day, maxima of DOD distribution will be more frequently located over the sources. This relationship seems to apply even over regions with quasi-permanent wind direction. For example,Ginoux et al.  showed that within the Bodélé depression, the DOD maximum lies precisely over some ephemeral lakes, although the wind direction over the depression flows consistently from the northeast.
 One of the most comprehensive studies of dust sources was realized by Prospero et al. using near-ultraviolet (nUV) measurements by TOMS between 1980 to 1992.Herman et al.  defined the TOMS aerosol index (AI) as a function of the ratio of the backscattering radiances at two wavelengths in the nUV. They showed that the TOMS AI can be used to detect dust events. Prospero et al. associated dust sources with the most frequent occurrence of TOMS AI greater than 0.7 over North Africa and 0.2 elsewhere. The difficulties in using TOMS AI to identify dust include the interference of other nUV absorbing aerosols, the sensitivity of TOMS to the aerosol vertical profile, and the presence of subpixel or underlying clouds. By restricting the use of TOMS AI to arid regions, the interference of clouds and other absorbing aerosols (e.g., black carbon) was minimized, and consequently, TOMS AI would be expected to be a good indicator of the presence of dust. Outside arid regions dust sources could not be unambiguously detected. M-DB2 does not suffer from these limitations, although it has its own limitations, in particular, it provides data only over bright surfaces. But the major advantage of M-DB2 products is that it can be used to make quantitative measurements of AOD, while TOMS AI cannot.
 Nonetheless the frequency of dust occurrence derived from TOMS AI and M-DB2 DOD should yield similar distributions over regions with overlapping retrievals. Although most dust sources identified byProspero et al.  are associated with paleolakes and depressions characterized by a deep layer of sediment, Zender and Kwon have shown that they can be subdivided depending on their response to precipitation anomalies. Some of these sources are supply limited, and their activity will depend on interannual alluvial recharge or modification of their surface crust. In making this performance comparison, we also use OMI in order to account for natural change of sources distribution over the decade that has elapsed between TOMS and M-DB2 recording dates. The OMI instrument was launched in 2004, and aerosol products are available up to 2006. The OMI aerosol index is calculated using the same wavelengths as for TOMS AI (seeTorres et al.  for details).
Figure 6shows the global distribution of the mean annual frequency of occurrence of M-DB2 DOD > 0.2, TOMS AI ≥ 0.5, and OMI AI ≥ 0.5. The frequency for M-DB2 DOD is calculated as previously described, but for the entire year rather than for each season. The TOMS and OMI AI FoO are calculated similarly by counting the number of days each year that AI > 0.5, divided by the total number of days with data, and converting into a percentage. The mean values are obtained by averaging the yearly FoO between 1980 and 1992 for TOMS AI, between 2004 and 2006 for OMI AI, and between 2003 and 2009 for M-DB2 DOD. InFigure 6, the overlap of different FoO for TOMS AI and OMI AI is informative considering that 2 decades separate their measurements. One major exception is over east China, where the 50% FoO isoline of OMI AI (lighter green isocontour) covers most of it, while the same isoline for TOMS AI (lighter blue isocontour) is limited to the Beijing area. This difference might be linked to the increasing trend of dust emission in some areas of eastern China as reported by Zhang et al. . They associated the trend in these areas to desertification of anthropogenic origin. More recently, Igarashi et al.  indicate that the increasing trend of dust emission in east China is due to an adverse combination of anthropogenic grassland degradation and drought. Another region with increasing AI is along the border of Uzbekistan and Kazakhstan. This may be associated with intense irrigation along the Syr Darya and Amu Darya [Micklin, 2007]. Conversely, in Botswana and northern Australia, AI > 0.5 was observed more frequently by TOMS than OMI instruments. This decreased frequency is contrary to a study of dust storms in Australia by Ekström et al. . They showed an increasing trend in the annual number of dust storms in continental and coastal regions of Australia in the last 20 years of the twentieth century that they attributed to increased drought. However, the dependency of AI on factors such as elevation, layer thickness, and the absorption properties of dust is as strong as the mass load [Ginoux and Torres, 2003]. These factors may be responsible for this apparent discrepancy between TOMS and OMI AI.
 Concerning M-DB2 dust sources, the TOMS and OMI AI envelop most of M-DB2 DOD shading. The regions where M-DB2 coverage is larger than OMI and TOMS are the high plains of the United States, the Baja California Peninsula, the Mediterranean basin, Kirghiz steppe of Kazakhstan, and the Australian Riverina. We might have also added to the list the southeast coast of India if the number of retrievals were not so low (cf.Figure 1). In 2007, the period not covered by OMI data, the western North American plains were particularly wet, but 2008 and 2009 were marked by dry-to-drought conditions [Cayan et al., 2010]. The drought in East Australia in 2009 has been linked to a very pronounced El Niño phase over the Pacific [Webb et al., 2006].
 On the other hand, some areas of TOMS AI > 0.5 do not overlap with M-DB2 FoO DOD > 0.2, most notably the region south of the Sahel in North Africa. These differences occur most frequently in the tropics where there is no M-DB2 retrieval (cf.Figure 1). In Botswana, both OMI and M-DB2 have much lower frequency of dust events than TOMS because the 1980s were much drier in southern Africa [Morishima and Akasaka, 2010]. In east China, OMI AI covers a larger area than M-DB2 shading, which in turn covers a much larger region than the TOMS AI 50% isoline. As the number of dust events detected from M-DB2 is quite low (cf.Figure 5), it is difficult to reach firm conclusions about these differences.
Prospero et al. have shown that dust sources are usually associated with topographical lows in arid regions where runoff and flooding have created lacustrine and alluvial sediments. Only the most prominent topographic features were characterized in their study because of the coarse TOMS resolution. With M-DB2 0.1° resolution, it is possible to make more precise attributions, in particular the linking of sources to land use and ephemeral water bodies.
 To link dust sources to hydrologic features, we use MODIS 0.01° resolution database (E. Vermote, personal communication, 2010), which provides data on shorelines, ephemeral water, and shallow and deep inland water features. We identify a dust source as “hydrologic” when there is at least one of these types of water bodies within a M-DB2 0.1° grid cell. Our method excludes any hydrologic feature less than 1 km wide. As most rivers, ponds, and lakes have smaller scale, we may be underestimating the amount of sources directly related to hydrology.
 We label a dust source as “anthropogenic” if it is associated with some form of land use (agriculture). We use the data set developed by Klein Goldewijk  (henceforth KG01) which provides globally the fraction of agriculture within every 0.1° grid cell relative to the end of the twentieth century. To determine the relative importance of climate and land use in dust emission, Tegen et al.  considered a source to be natural if there is less than 5% land use. A similar threshold was used by Ginoux et al. . However, most desertic areas in the KG01 data set have 5% land use, and it is not realistic to assume that most desertic sources are anthropogenic. On the other hand, above 30% land use the spatial distribution is relatively similar. This may be explained by the fact that once an area is found to be suitable for agriculture, most of the land will be rapidly developed for such use. Therefore, we adopt a value of 30% as the threshold land use to separate natural and anthropogenic sources. The sensitivity of our computed dust emissions to land use percentage is discussed in section 6.
 In the following eight figures the relative frequency of DOD > 0.2 on a seasonal or annual basis is shown for different continental regions. The selection of a particular season is based on the maximum intensity of the sources over that region. It should be noted that the scaling of FoO varies between figures to improve clarity. In addition, dust sources may vary considerably between seasons. Because of space limitations, we only show the peak seasons of dust activity. The exception is North Africa, for which we show the annual distribution.
 The figures show the associations with three source types: hydrologic, dust linked to various water features as discussed above; natural, dust emitted from land surfaces where land use is less than 30%; and anthropogenic, sources where land use exceeds 30%. The dominant source designation is carried out as follows: If there is a hydrographic feature in the grid cell, it is designated as “hydro” source. If it is not “hydro” and if land use is less than 30%, it is “natural.” If it is not “hydro” and land use is greater than 30%, it is “anthropogenic.”
5.4. North Africa and Europe
 The annual mean distribution of FoO AOD > 0.2 over North Africa is shown in Figure 7. A major difference from the results of Prospero et al.  is the large source of dust throughout much of the southern Sahel (black contour labeled A in Figure 7). However, Prospero et al.  removed the Sahel region from their study because TOMS AI could not distinguish between biomass burning aerosols and dust. We also note in Figure 7 the southern Sahel sources are overwhelmingly anthropogenic, and there is a clear separation between natural dust sources in the Sahara and anthropogenic dust in the southern Sahel. The sources in the Atlas Mountains (zone F in Figure 7) and along the Mediterranean coast are also mostly anthropogenic.
 There are limited in situ data over the Sahel, but they all suggest that dust emissions are related to land use. Gill  reported measurements in the 1950s showing that playas and ephemeral lakes were reactivated by overgrazing and cultivation in Senegal (location 1 in Figure 7), as well as from Lake Faguibine in Mali (blue spot in location 3 at the border with Mauritania). Analyzing thousands of years of dust deposition in the mouth of the Senegal River, Mulitza et al.  found a sharp increase after the advent of commercial agriculture in the Sahel, about 200 years ago. Gillies et al.  have studied intense dust haze events emitted from alluvial sediments of the Inland Delta of the Niger River (location 3) near Mopti in Mali. These sediments are deposited by seasonal flooding from the Niger River. These sediments have a large percentage of silt and clay and are generally heavily crusted except where disturbed by herds [Nickling and Gillies, 1993]. Using surface visibility data, N'Tchayi Mbourou et al.  reported a continually increasing presence of dust in the Sahel since the 1950s, particularly in the western Sahel. A recent analysis of this data set by Klose et al.  suggests that dust observed in the Sahel is primarily windborne dust transported from the Sahara. On the other hand, Bou Karam et al.  studied several cases of dust storms generated within the monsoon flow over the Sahel, and Lyngsie et al.  found that dust collected in northern Ghana had a local origin.
 The Senegal River Basin (location 1 in Figure 7) appears as an anthropogenic source with FoO up to 60% of days per year. Niang et al.  analyzed 50 years of visibility data and aerial photos along the Senegal River. They found a continuous disappearance of forest from 1954 to 1992, a time span that included the severe droughts of the 1970s and 1980s. During the following years precipitation was closer to normal; water erosion increased, which produced gullying, bank erosion, and badlands, which in turn resulted in increased dust production. These observations are consistent with those of Mulitza et al. , who associated increased offshore sediment deposition with the onset of agriculture in the region. We lack similar information for the Niger River, but we would expect the same sequence of conditions: deforestation followed by water and wind erosion. If confirmed, it would suggest that dust sources in the Sahel are largely controlled by river streamflow and soil disturbance.
 Outside the Sahel, major sources in Figure 7 have been identified and described by Prospero et al. . These include major depressions (Bodélé, location 7, and Qattarah, location 17), large basins with sand seas (Erg of Bilma, location 8; Erg el Djouf, location 10; Grand Erg Occidental, location 13; Grand Erg Oriental, location 14; and Libyan Desert, location 15), ephemeral lakes (Sebkhet te-n-Dgâmcha, location 11; Chott el Jerïd, location 19; Chott Melrhir, location 20; and lakes in the Tiris Zemmour region, location 12), and the Nile River Basin (location 16), all of which are essentially natural sources. Additional sources associated with ephemeral lakes can be identified inFigure 7, such as Chott el Hodma (location 21) and Chott ech Chergui (location 22) in the Atlas Mountains (location F). Mahowald et al.  have shown the importance of the hydrological cycle on modulating dust emission in the zone of Chotts. In addition to these large natural sources, smaller anthropogenic sources can be identified in coastal Morocco (location 23), Tunisia, Libya, and Egypt.
 The Bodélé depression (location 7 in Figure 7) has been studied extensively, including during the BoDEx field campaign [Washington et al., 2006; Todd et al., 2007]. Prospero et al.  described it as one of the most intense dust sources in the world. The frequency and intensity of dust emissions from the Bodélé has been related to a Venturi effect of the Harmattan winds passing between the Ennedi (location C) and Tibesti (location D) mountains [Washington et al., 2006]. In Figure 7, we see additional sources (location 5) associated with alluvial fans and wadis on the flanks of the Ennedi (location C) and Ouaddai highlands (location B). The alluvial fans in this region are the sources of weathered sedimentary material which is carried down to the Bodélé (location 7) and even the Erg of Bilma (location 8), constantly replenishing these sources with fine soil particles [Wright, 2001]. Schepanski et al.  also identified these flanking fans as dust sources. Alluvial sediments (location 9) are also clearly identified on the southern flank of the Aïr and the Ahaggar (location E) mountains. These sources are sensitive to the hydrological cycle as well as to effects of mesoscale winds intensified by the orography.
 Dust activity is seen in Figure 7 along the Mediterranean basin in Andalusia (location 24) and Cyprus (location 18). These sources reach a maximum activity in summer, with maximum FoO over the fluvial plains of the Guadalquivir and Segura Rivers in southern Spain. Dust from these sources is mainly associated with agriculture, and dust tends to channel through and flow down the river valley [Fernandez et al., 2000]. Desertification in the western Mediterranean basin has been documented for quite some time and appears to have been triggered by climatic variability and demographic disequilibrium and the associated changes in agricultural practice [Puigdefábregas and Mendizabal, 1998]. In summer, dust sources are also apparent in the Konya plain (cf. third panel in Figure 4), which were previously identified as the hot spot of wind erosion in Turkey [Berktay et al., 2006; Avci, 2011].
5.5. Middle East
 The distribution of FoO with DOD > 0.2 for the Middle East is shown in Figure 8 for MAM. FoO is higher than 20% over most of Mesopotamia (location 11) and is composed of a mixture of anthropogenic, natural, and hydrologic sources. As far back as the 1980s, the region was described as a major source of dust [Middleton, 1986]. The dust from the region between the Tigris and Euphrates is mostly natural in Iraq but anthropogenic in Syria. There is also a distinct contrast at the border of Iraq with Saudi Arabia and Iran where dust is anthropogenic. The maximum frequency (FoO > 60%) is located over the farmland region northeast of the city of Ar Raqqah (Syria) in the northwest of region location 11, which was described by Walker et al. as generating anthropogenic dust plumes. The highest frequency along the border of Syria and Iraq corresponds to several sabkhas (Arabic for salt flat): Albu Gharz, al Burghuth, and Ar-Rawda. In Saudi Arabia (location 9), there is a mixture of anthropogenic and hydrologic sources, but they are essentially aggregated around three wadis (Arabic for dry riverbed): Al Batin, Al-Rimah, and Al Sahba.Fryberger et al.  described eolian erosion from these wadis, as well as from the sabkhas, with a peak emission in June. In the Rub' al Khali sandy desert (location 8), the sources are sparse, except for the very large Sabkha Matti in the United Arab Emirates, which extends from the Emirates into Saudi Arabia. The sabkha interfingers into sand dunes, offering a source of sand which efficiently sandblasts the sabkha surface to generate dust emission as observed by Alsharhan and ElSammak . Dust storms in the area are becoming an environmental problem [Abdelfattah, 2009].
 There are many other sources in the Middle East. We note in particular a cluster of anthropogenic and hydrologic sources along the Jordan River, particularly on the east side (location 10) which corresponds to the Wadi Araba Desert characterized by Saqqa and Atallah . Several studies have indicated that the diversion of water from the Jordan River has induced wind erosion of desiccated sediments in the Paleolake Lisan basin [Gill, 1996; Ghazleh et al., 2011]. In Yemen, large dust sources are associated with river fans at the base of the coastal escarpment in the Hadramawt (location 7).
 One prominent source is situated along the west coast of Iran (location 13), as previously noted by Middleton  and Littmann . The northwestern part is anthropogenic, and the southeastern part is natural. The other major sources in Iran are associated with large salty lakes, such as the southern shore of the Urumia Lake (location 12), or in the Hamun-i-Mashkel (location 14) and the Dasht-e Kavir (location 16) Deserts. These deserts have been previously identified as dust sources byMiddleton . More recently, Rashki et al. have indicated that due to land use change and desiccation of lakes in the Hamun-i-Mashkel, the frequency and severity of dust storms have been significantly increased. Because of water diversions, Urumia Lake is becoming a new source of salt dust [Golabian, 2011; Zarghami, 2011] much like the Aral Sea today.
 The plains between the Caspian and Aral Seas are largely irrigated for agriculture and thus qualify as active anthropogenic dust sources. Specific sources are the delta of the Atrek River (location 18) and the Turan plain (location 19). The dramatic decrease in the size of the Caspian Sea because of water diversions has lead to rapid exposures of formerly inundated land [Dickerson, 2000] which have now become dust sources. The diversion of river water for irrigation has greatly reduced river flow and is the fundamental cause of the desiccation of the Aral Sea [Micklin, 2007, 2010]. The Aral Sea was formerly one of the largest lakes in the world (area 68,000 km2) but is now reduced to 10% of its original size. Large areas of the Aral Sea are now active dust sources (location 20), in agreement with in situ measurements by Wiggs et al. . Darmenova and Sokolik  showed the importance of feedbacks between dust emission and meteorology over the Aral Sea. The authors noted that such feedbacks add further complexity to the quantification of the anthropogenic dust fraction in the region. On the west side of the Caspian Sea, the sources are limited to small sections along the coastal region in the Qobustan area (location 17), south of Baku. The region has the largest concentration of mud volcanoes in the world, which emit mineral aerosols with large amounts of gases [Kopf et al., 2010].
5.6. East Africa
 In northeast Africa, the dust sources are aggregated into six arid or semiarid areas (Figure 8): the Chalbi Desert and semiarid northeastern province of Kenya (location 1), the coastal desert of Somalia (location 2), the arid Nogal Valley (location 3), the Danakil Desert in the Dafar Depression of Ethiopia (location 4), Lake Tana of Ethiopia (location 5), and the coastal region of northeast Sudan (location 6). The Chalbi and Danakil Deserts were paleolakes at about the same time as the Bodélé depression was a lake [Abell and Nyamweru, 1988]; with changing climate the lakes became dust sources [Nyamweru and Bowman, 1989], as previously noted by Parkinson  and Hemming and Trapnell .
5.7. Indian Subcontinent
Figure 9 shows FoO distribution over the Indian subcontinent in MAM when DOD is high over all of northern India (Figure 4). The dust is largely attributed to land use with a widespread contribution associated with ephemeral water bodies ranging in scale from the major rivers to small lakes. Some seasonal lakes may be so dense as to occupy an entire region, such as in the Rann of Kutch (location 8). Dust sources occupy the entire Indo-Gangetic basin (locations 1, 2, and 3), which is characterized by intense agricultural activities as well as persistence of dust transported from desert regions of western India [Prasad et al., 2007].
 The highest frequency is observed in the Rajasthan province (location 2) with maxima (FoO > 70%) along the Ghaggar River, which flows intermittently only during the monsoon season (June to September). The Rajasthan Desert is considered as a significant dust source of southwest Asia [Pandithurai et al., 2008], and Ramachandran et al.  indicate that increased wind speed over the Rajasthan Desert is a factor in increasing optical depth over parts of India over the past decade. Gill previously indicated that human-influenced desertification processes have resulted in wind erosion and deposition of sediments in saline lake basins in Rajasthan. Other agricultural areas include the Indian Plateau where FoO is in some areas greater than 20%.
 In Pakistan, the most pronounced maximum is in the Lakki Marwat district over the fluvial plain of the Karram River, a tributary of the Indus (location 3). Dust events yield FoO greater than 40% along the Makran coast of Pakistan (location 7) and more than 70% FoO in the fluvial plain of the Dasht River near the border with Iran. Using TOMS aerosol index, Goudie and Middleton classified the Makran coast as one of the major global dust sources. The Hamun-i-Mashkel ephemeral lake (location 6) was identified previously byMiddleton as a dust source, and M-DB2 indicates up to 50% FoO during spring.
 In Afghanistan, there are two areas of dust activity. One occupies the front range of the Hindu Kush (location 4), which is strongly incised by many rivers feeding into the Helmand River with some irrigated agriculture along Highway 1 between Farah in the west to Kandahar. The other is formed by dust from seasonal lakes within the Sistan Basin (location 5): the Hamoun-i Sabari, Hamun-i Puza, and Gaud-i Zereh in Afghanistan and the Hamin-i Helmand in Iran. The extent and volume of the hamuns varies substantially from season to season and from year to year. They expand during the spring and reach a maximum size in late May and June and then shrink due to high evaporation and low inflow [Whitney, 2006]. On the basis of dust storm frequency, Middleton  ranked Zabol among the dustiest places on Earth. The Helmand Basin has recently experienced an unusually prolonged series of droughts since 2000, and as one of the windiest deserts in the world, it produces dust plumes that are hundreds of kilometers long and which are frequently captured in spectacular satellite images [Whitney, 2006].
5.8. East Asia
 In China (Figure 10) the largest natural sources are associated with basins (“pendi” in Mandarin). They include the Taklamakan Desert of the Tarim Pendi (location 1), the Qaidam Pendi (location 2), and the Turpan Pendi (location 10). A long series of natural sources are stretched along the Hexi corridor, in the Gansu province (location 3) at the base of the Tibetan plateau; these sources are associated with fluvial fans [Derbyshire et al., 1998]. Except for some areas in the Gobi Desert of Inner Mongolia (location 9), all other sources are essentially anthropogenic. Xuan and Sokolik  found that human activities, mainly farming, overgrazing, and water usage, have likely been responsible for the expansion of dust sources in northern China. Igarashi et al.  add that drought has been also a contributing factor. Gong et al.  showed that although desertification has increased by only a few percent in China, it has generated disproportionately large areas of enhanced dust emissions. In agreement with their study, Figure 10 shows anthropogenic sources mostly in the deserts of Inner Mongolia (location 9), on the Hulun Buir plain (location 8), on the northeast China plains (location 7), within the Junggar Pendi (location 12), and on the margins of the Tarim Pendi (location 1). The largest anthropogenic FoOs (between 10% and 25%) are distributed over the Junggar Pendi (location 12). Although there are scattered sources outside the identified areas in Figure 10, dust activity is relatively low with FoO less than 10%. Kurosaki and Mikami  have established over East Asia the geographic distribution of dust outbreaks and floating dust FoO from visibility data. Our results appear to agree with their study not only in the distribution of maxima but also in the values of FoO. The similarity of our results is also apparent in agricultural or industrialized areas, such as along the Wei and Yellow Rivers (location 4), in the north China plains (location 6), and around Hongze and Gaoyou Lakes in eastern China (location 5). This is also consistent with Wang et al. , who find that dust storm frequency does not exceed 8 days per year in northern China, even where there are high levels of human activity.
 In Mongolia, there are dozens of small sources associated with pasture, lakes, or alluvial fans. The sources are generally small with low FoO except in the Great Lakes depression (location 11), where FoO > 10% around Lakes Chjargas and Char Us. In the southern part, along the Gobi Desert, FoO varies between 5% and 10%. This seems to agree with the analysis of data from 47 meteorological stations in Mongolia by Natsagdorj et al. . They found that only in the southern Gobi Desert and semidesert areas could the frequency of dust storms reach 10%; elsewhere, it is less than 5%.
 The Balkhash-Alakol depression in eastern Kazakhstan (location 13) is a significant source of anthropogenic dust.Gill  indicated that Lake Balkhash has been rapidly desiccating since 1970 after completion of a dam on the Ili River. Over the eastern part of Lake Balkhash and the entirety of nearby dry lakes, the FoO is greater than 50%. Abuduwaili et al. have studied Lake Ebinur located on the eastern part of the Dzungarian basin (location 12) in a narrow pass connecting with the Balkhash-Alakol depression (location 13). As a result of human-induced desiccation, the dry lake bed is now the source of intense dust storms with a peak frequency in spring. Chemical analyses of dust samples around Lake Ebinur indicate a high level of potentially toxic trace elements [Liu et al., 2011]. Within the depression, FoO is mostly anthropogenic with values between 10% and 25%. The impact of human activities in the area has been investigated by Kezer and Matsuyama , who found that river runoff draining into Lake Balkhash has decreased by half since 1970 due to human activity. In fact, comparable reductions were found for most tail-end lakes in flat areas of central Asia [Bai et al., 2011].
5.9. North America
 Most dust activity over North America (Figure 11) is centered in two western areas separated by the continental divide. One area occupies the high plains (location 11) on the east side of Rockies and is essentially anthropogenic. On the west side of the divide, the anthropogenic and natural sources are intertwined. In the Sonoran Desert (location 1), sources on the west side of the Gulf of California are mostly natural, and on the east side, sources are anthropogenic.
 The high plains (location 11 in Figure 11), which extend from Montana to southern Texas, are the largest dust source in North America, and the dust is almost entirely anthropogenic in origin except for a few ephemeral lakes. This semiarid and subhumid region accounts for 60% of wind erosion in the U.S., with the highest frequency located in the southern plains of Texas, which experience 50 dust days per year, the national maximum [Hagen and Woodruff, 1973]. Our result differs from Prospero et al. , who did not find any significant dust activity in the high plains from TOMS data covering the 1980s. But an earlier study based on visibility data from 1940 to 1970 by Orgill and Sehmel  did show a maximum reduction of visibility along the high plains, with a peak in the southern great plains. Cook et al.  have reconstructed drought cycles over North America from tree rings. They reported severe drought in the midwest and high plains for the 1930s, 1950s, and 2000s, while the 1980s were not particularly dry or wet. This suggests that dust source activity in the high plains is modulated by precipitation variability. Such a dependency has been previously shown to exist in the southern part of the high plains by Stout and Lee . With projected increase of severe drought in the southwest [Seager and Vecchi, 2010], this region may experience an increase in dust events in the future.
 An interesting result drawn from Figure 11 is that major river basins are potential dust sources, although relatively weak. These include the Snake (location 6), Colorado (location 8), Pecos and Rio Grande (location 10), and Big Sioux (location 12) Rivers and the lower Yellowstone Valley (location 13). Dust activity in some of these basins has been previously reported [Lee et al., 2009; Munson et al., 2011]. In fact, there is a remarkable similarity between Figure 11 and the figure presented by Nordstrom and Hotta  showing the locations of cropland in the U.S. that have the greatest potential for wind erosion.
 In the Columbia plateau, Nordstrom and Hotta  indicated that dust is related to dry conditions and agricultural practice. Each fall after harvest, half of the dryland soils are bare due to the 2 year crop rotation system, while the other half is mostly dry and sparsely vegetated rangelands [Claiborn et al., 1998].
 Some anthropogenic dust sources are observed along the Coast Ranges in the southwest part of the San Joaquin Valley, California. M-DB2 sources in the valley (location 3) are essentially anthropogenic and localized in the southernmost part near Bakersfield. There is one natural hot spot over the Carrizo Plain, which includes Soda Lake, shown as a hydrologic source inFigure 11. Nordstrom and Hotta  indicated that much of the dust produced from soil erosion in California comes from desert environments, but cropland is also prone to dust generation, such as in the same region of the Central Valley where agriculture is industrialized and the climate is semiarid Mediterranean type with a long, dry summer and fall. Fugitive dust from intense agricultural activities is the primary constituent of aerosols in the southern San Joaquin Valley [Chow et al., 1992, 2003].
 Our results reinforce the conclusions of previous studies in which it was shown that anthropogenic dust is significant in North America [e.g., Neff et al., 2008]. But there are also many natural sources in North America. Many are distributed within the Black Rock and Smoke Creek Deserts (location 4), Great Salt Lake Desert (location 7), Mojave Desert (location 2), and Chihuahuan Desert (location 9). The Black Rock Desert was part of Lake Lahontan in the Pleistocene, and the depression is now composed of multiple ephemeral lakes. Similarly, the Great Salt Lake Desert was part of Lake Bonneville in the Pleistocene. In these deserts, FoO maxima are localized on or near the playas, with values greater than 20% covering Sand Spring Salt Flat and the southern part of Lakes Winnemucca and Pyramid. Peak activities are in spring. The generation of dust storms from these playas has been mentioned by Gill  and studied in detail by Lewis et al.  and Hahnenberger and Nicoll .
 The source characteristics of Chihuahuan Desert (location 9) dust outbreaks have been studied by Rivera Rivera et al. . They showed that although playa deposits and alluvial deposits dominate the dust sources, about 23% of them are agricultural lands. This partitioning corresponds to our results.
Figure 11 shows many sources, either natural or anthropogenic, related to ephemeral water bodies. An example is Owens Lake in California (location 2) which was desiccated by water diversions of the Owens River into Los Angeles Aqueduct since 1913 [Gill, 1996]. Goose Lake (location 5) at the border between Oregon and California is a quasi-permanent dust source in M-DB2 data.Gill  found that the desiccation of Goose Lake, among others, has lead to blowing plumes of salt dust. Similarly ephemeral lakes in the Great Salt Lake Desert (location 7), the Mojave Desert (location 2), and the Sonoran Desert (location 1) are sources of dust.
5.10. South America
 The FoO distribution DOD > 0.2 for DJF over South America is shown in Figure 12. The largest natural sources of dust are located in the Atacama Desert of Chile (location 12), followed by the Nazca (location 14) and Sechura (location 15) Deserts of Peru. In Argentina, the FoO distribution matches remarkably well the zones of aeolian landforms described by Zárate and Tripaldi ; all sources are of anthropogenic origin, except on the eastern flank of the Andes (location 8).
 The dust sources in Patagonia are often associated with major river basins: sections of the Rio Negro from Neuquén to the Atlantic in the Rio Negro province (location 6), most of the Chubut (from Lake Colhue Huapi) and Chico Rivers in the Chubut province (location 5), and the lower section of the Deseado River in the Santa Cruz province (location 4). Pasquini and Depetris  studied the discharge trends and flow dynamics of South American rivers from the early 20th century to the beginning of the 21st century. They found a significant decrease in the discharge of all the rivers that we identify as dust sources; in contrast, they found increasing flow trends for the rivers not appearing as dust sources in Figure 12 (e.g., the Santa Cruz in Santa Cruz province). This would seem to suggest an influence of climate variability on dust sources in Patagonia. However, it has been suggested that sheep ranching is largely responsible for the desertification of Patagonia and is the cause of the observed doubling of dust in Antarctic Peninsula ice cores during the twentieth century [McConnell et al., 2007]. Due to the tendency of herds to concentrate around water sources, riparian areas and wetlands are heavily impacted by grazing. Consequently, dust sources in Patagonia may be characterized as being anthropogenic both by direct disturbance of soil cover and by the indirect effect of climate change. Similarly, in the Magellan region (location 1), ranching is important, and again, dust sources are observed along the Gallegos River.
 Patagonia is also a region of known glaciogenic dust sources [Li et al., 2008, 2010]. Sugden et al.  suggest that glacial lakes San Martin, Viedna (location 2), and Pueyrredon (location 3) are linked to the variability of dust concentration in Antarctic ice cores over 80,000 years. Gassó and Stein  report on a dust event originating from this region that was subsequently traced to the Antarctic 48 h later. It is remarkable to observe in Figure 12 that these small sources have apparently been active over such a long period.
 Other sources of dust in Argentina are associated with salt lakes: Laguna Salada (location 9), Laguna Mar Chiquita (location 10), and lakes in the Salinas Grandes Desert (location 11). The water level of the Laguna Mar Chiquita varies considerably, and during low-level stages the development of dust storms has been observed [Troin et al., 2010]. Prospero et al.  found a weak but persistent source of dust in the Bolivian Altiplano. Here we find much reduced activity. Indeed, the only place with FoO > 10% is over the northern half of Lake Poopo (location 13). A possible explanation is that Figure 12 corresponds to austral summer, the only period with precipitation over the Altiplano [Garreaud and Aceituno, 2001]. In austral spring, M-DB2 shows a dozen more sources associated with ephemeral lakes over the Altiplano.
5.11. Southern Africa
 The FoO distributions of DOD > 0.2 over southern Africa are shown for austral spring and summer in Figure 13. The figures show considerable variation between seasons. Activity develops weakly on the western regions in austral spring and increases strongly in summer, spreading into central regions. The major exception is the Namib Desert (location 1), which is active during most seasons. Using Sea-viewing Wide Field-of-view Sensor (SeaWiFS),Eckardt and Kuring  have shown that dust sources of the Namib Desert are associated with either salt pans or dry river beds, and their supply of dust is maintained by fluvial landforms and associated hydrology.
 Silty deposits are widespread on the eastern margin of the escarpment bordering the Namib Desert. These deposits are locally produced weathering detritus and allocthonous dust blown in from the western Kalahari (location 10) [Eitel et al., 2001]. These deposits appear as an elongated dust source (location 12) in Figure 13a, activated by easterly winds in December, January, and February. During that season, FoO is greater than 20% in some areas. In other seasons, this elongated source is inactive.
Bryant et al.  have shown that the Kalahari Desert (location 10), including the Makgadikgadi Pans (location 9), is influenced by the extent and frequency of lake inundation, sediment inflows, and surface wind speed variability. They suggested that TOMS aerosol optical depth was unreliable because it showed peaked activity over the Makgadikgadi from August to October. But our results also indicate a maximum FoO over the Makgadikgadi (location 9) from September to October. On the other hand, dust activity over the Etosha Pans (location 11) and the Kalahari (location 10) is greatest in the December–February period, in agreement with their study. An explanation of this discrepancy may be related to the strong interannual variability of inundation, which shuts down dust emission [Mahowald et al., 2003], and the fact that we analyze different periods.
 The other significant source areas in South Africa are the ephemeral lakes in Bushmanland (location 3), the Swartland north of Cape Town (location 2 in Figure 13), the Highveld region around the Bloemhof Dam (location 4), and the Namaqualand Desert (between the Namib Desert (location 1) and Cape Town (location 2)). The anthropogenic nature of these sources has been studied elsewhere [Soderberg and Compton, 2007]. Meadows  has documented the wind erosion of sandy agricultural soils of the Swartland; Wiggs and Holmes  have studied wind erosion in the Highveld; and Botha et al.  have shown that the combination of dry climate, strong winds, and especially land degradation have contributed to wind erosion in the Namaqualand.
 We also found active anthropogenic dust sources in Zimbabwe (Hippo Valley, location 5) and Mozambique (Cahora Bassa reservoir, location 8). But these sources are only active in austral spring.
 Dust sources in Madagascar have not been studied previously, although extensive soil erosion due to deforestation has been documented [Goudie and Boardman, 2010], and wind erosion has been suggested in southern Madagascar (location 6) by Feddema . December through February is the rainy season, but rainfall is essentially concentrated in the east and north, such that dust activity is located in the semiarid southwest of Madagascar (location 6). Before the rainy season some areas of northern Madagascar (location 7) appear as active dust sources.
 In Figure 14, Australia shows a large spatial change in dust source activity between austral spring, when northern sources are most active, and summer, when there is less activity and it is centered in the southeast. Dust sources in Australia are associated with either hydrologic features or land use. Based on the KG01 land use data set, the percentage of land use in Australia is generally higher than 50% everywhere and often reaches 75% or more. The land use is for pasture except in the SW and SE (Murray region), where cropland is more intensive.
 The dust sources are mainly located in eastern Australia: Queensland, Northern Territory, South Australia, New South Wales, and Victoria.
 The most active sources are located within the Lake Eyre Basin (location 4), as previously shown by Prospero et al. . Bullard et al.  found that in the basin 60% of dust plumes originate from hydrologic features with 30% from ephemeral lakes. From Figure 14, it appears that the Eyre Lakes (north and south) themselves are weakly active dust sources compared to the feeding creeks on the north and east sides where FOO > 20%. On an annual basis, the largest source with the highest frequency over the entire Australian continent is in channel country, at the mouth of the Warburton River feeding North Lake Eyre. Dust emission in the channel country has been described by multiple studies [Nickling et al., 1999; Butler et al., 2001, 2005], and Prospero et al.  have described Warburton Creek as a major dust source in Australia. In the Lake Eyre Basin, there are dozens of smaller lakes, some of them active while others are not. Some are active all year long (e.g., Lake Yamma Yamma), while others are active for one or two seasons (e.g., Lake Frome, active in SON). The difference may be linked to their geomorphology and to river discharge. The soils around Lake Yamma Yamma are composed of clay and fine sediments and are transected with wide expanses of braided fluvial channels [Fagan and Nanson, 2004]. In contrast, Lake Frome is only occasionally fed through the Bullow Overflow during austral summer flooding [McTainsh, 1989]. In the Lake Eyre Basin dust activity is greatest and most widespread in austral spring. In the Simpson Desert (location 5 in Figure 14) dust activity is most frequent in austral spring and summer but is limited to only a few spots for the remainder of the year. The Simpson Desert is a sand desert where dust is produced by abrasion of the sand mantle composed of fine clays and iron oxides, not by ejection of fine particles by sandblasting of alluvium [Bullard et al., 2007]. Although the amount of erodible material is limited, the Simpson Desert can yield very large amounts of dust during major events [Knight et al., 1995].
 The dust sources of the Murray-Darling are aggregated in three clusters: the Victorian Big Desert (location 1 inFigure 14), the irrigated farmland of Riverina (location 2), and the Barwon-Darling Basin (location 3). The Murray-Darling River systems erode fine particles from the uplands and carry them downriver into the arid zone where they served as one of the major Australian dust sources in the present and geological past [Hesse and McTainsh, 2003; Li et al., 2008; Marx et al., 2009]. In the Miocene, the Victorian Big Desert was a shallow sea which since has been slowly filled with sediments. Since European settlement began in the region, the hydrological regime has been disrupted by the increasing demand of water for agriculture and clearing of land, which has led to significant increase in dust deposition on a millennial scale [Marx et al., 2011]. As a consequence of diversion, the ephemeral lakes within the region were last filled in 1976 [Wevill and Read, 2010]. The area is now part of a network of parks, including the Wyperfeld National Park. Within the Murray-Darling basin, dust events are more widespread in the southern part in austral summer and in the Barwon-Darling basin in austral spring.
 It should be noted that the period of M-DB2 data overlaps the 2001–2007 Australian drought. During this drought, the inflow into the Murray-Darling River system was reduced by a factor of 3, reaching a historical low [Cai and Cowan, 2008]. As a consequence of frequent dust events the Darling River from the Barwon Basin to the Victorian Big Desert appears as a long narrow strip (location 3 in Figure 14). In general, the spatial distribution of rainfall in Australia is controlled by El Niño/La Niña–Southern Oscillation (ENSO) and monsoon variability [Marx et al., 2009]. Using the Australian Land Erodibility Model, Webb et al.  have shown that during El Niño conditions, there is increased wind erosion in central and southeastern Australia, while during La Niña years the sources are shifted to the southwestern regions. They provided maps of wind erosion susceptibility for dry and wet years. In dry years, their results are quite similar to Figure 14, with high susceptibility in the Lake Eyre basin and the Murray-Darling basin and low susceptibility in the west.
 In Northern Territory and Queensland, dust events are most frequent in spring. Their frequency decreases in summer, and only Lakes Tarrabol and Sylvester in the Barkly Tableland (location 7 in Figure 14) are still active from June to August. This was shown previously by Prospero et al. . The M-DB2 period covers two pronounced El Niño periods (2002–2004 and 2009–2010), years which favor dust activity in Northern Territory and Queensland [Webb et al., 2006]. This may explain why this large source area location 6 is located on the lee side of the Great Dividing Range. However, if we had included the strong La Niña 2010–2011 years, the results may have shown much reduced mean dust activities in the east and more in the west, based on the results of Webb et al. . Indeed, Bullard and McTainsh  have shown a strong relationship between ENSO cycles and dust emissions and sediment supply.
6. DUST EMISSION
 Dust emission is mainly initiated by saltation and sandblasting processes which have been parameterized based on laboratory measurements and field studies. The main parameters include the soil granulometry, cohesion, moisture, and the surface roughness. These parameters are implicitly expressed in a threshold velocity of wind erosion, which is the minimum velocity to initiate dust emission. Different parameterizations are available, and we use the simple expression of Ginoux et al.  where the dust emission Fp is calculated as follows:
where C a dimensional factor, S is the fraction of dust source, u10m is the horizontal wind speed at 10 m, and ut is the threshold velocity for wind erosion. The fraction of dust source Sis assumed to be proportional to the seasonal M-DB2 FoO.
 Dust emission is calculated using the 3-hourly instantaneous 10 m wind speed resulting from a 1 year simulation (2005) with the Geophysical Fluid Dynamics Laboratory C360 High Resolution Atmospheric Model (HIRAM) described byZhao et al. . The C360 configuration consists of 360 × 360 grid points on each face of a cubed sphere grid topology covering the Earth [Putman and Lin, 2007]. The size of the model grid varies from 20 to 30 km. Compared to 10 other general circulation models, HIRAM has the lowest root-mean-square errors for several meteorological fields including winds [Zhao et al., 2009].
 The dynamical processes generating u10m intense enough to overcome utcover a large range of scales: synoptic depressions, low-level jets and cold pools of mesoscale convective systems, and microscale dust devils and dusty plumes [Knippertz and Todd, 2012]. Most global dust models have a spatial resolution of the order of 100 km; consequently, they can only explicitly resolve synoptic systems but not smaller-scale processes. The simulation of dust storms associated with cold pool outflows from moist convection (so called “haboobs”) necessitates resolution of downdrafts within convective clouds. Resolving such small-scale processes can only be achieved in regional models. Global models with coarser resolution can attempt to simulate them through paramaterizations, but such an approach introduces uncertainties associated with each introduced parameter. In addition,Marsham et al.  have shown that the inclusion of parameterized moist convection into a regional model produces substantially fewer haboobs than when solved explicitly. For microscale dust devils, Koch and Renno have developed a parameterization which appears to lift significant amounts of dust, but the results have only been tested over a limited area in Arizona. Considering the difficulty of parameterizing these small-scale processes and the lack of data to constrain these parameters globally, we do not include any parameterization of convective vertical downdraft. This means that we are not able to include dust emission from haboobs which have been studied in West Africa [Bou Karam et al., 2009; Marsham et al., 2011], the Arabian Peninsula [Miller et al., 2008], Iraq and northwest Iran [Abdi Vishkaee et al., 2012], Australia [Strong et al., 2011], and North America [Idso et al., 1972; Chen and Fryrear, 2002]. The estimated contribution of these haboobs to dust emissions varies from 9% in Australia [Strong et al., 2011] up to 67% in West African monsoon [Bou Karam et al., 2009].
 Another uncertainty in equation (1) is associated with the threshold friction velocity, ut. Combining M-DB2 data with results from a high-resolution mesoscale model,Draxler et al.  showed typical values of ut over the United States to be around 60 cm s−1 over deserts and 100 cm s−1 over cultivated areas, such as the high plains. These results correspond to the values suggested by Gillette and Passi  for mixed barren lands (65 cm s−1) and pasture and range in good conditions (100 cm s−1). Converting these surface friction velocities to wind speed at 10 m, we impose ut = 6 and 10 m s−1 for smooth (natural and hydrologic sources) and vegetated (agriculture or range) surfaces, respectively. These values correspond to the range of values (6.5 to 13 m s−1) reported by Helgren and Prospero  for western Sahara. In the next section, we will test the sensitivity of dust emission to ut over vegetated surfaces.
6.1. Emission and Vegetation
Ginoux et al.  have developed a 1° resolution dust source inventory with preferential locations in topographic depressions (TOPO). The inventory includes a vegetation mask that excludes all sources for all ecosystems except bare ground. This inventory has been extensively used and evaluated [e.g., Cakmur et al., 2005]. As discussed in Ginoux et al. , a value of C = 1 μg s2 m−5 provides the best agreement with observations. Here we use their inventory to calculate the annual dust emission using HIRAM wind speed u10m. This yields an annual global emission of 1223 Tg yr−1 from bare ground. This value is lower than the value of Ginoux et al.  but close to the median value (1123 Tg yr−1) derived by Huneeus et al.  in the comparison of 15 global dust models. By considering relative emission between continents, we obtain similar results to those calculated by Ginoux et al.  using Ginoux et al.'s  sources.
 We then scale the C value to obtain also 1223 Tg yr−1when using M-DB2 FoO as source fractionS and the vegetation mask of Ginoux et al. . This calculation gives C = 1.9 μg s2 m−5, which is double the C value determined by Ginoux et al. .
Figure 15a shows the global distribution of annual emission using TOPO (C = 1 μg s2 m−5, ut = 6 m s−1, and S from Ginoux et al. ). Figure 15bshows also the global distribution of annual emission but using the M-DB2 FoO forS, C = 1.9 μg s2 m−5, and ut = 6 m s−1 over natural sources and 10 m s−1 over land use sources. With the introduction of vegetated surfaces (Figure 15b, blue shading), many new sources appear. The most intense are located in Kazakhstan near the Aral Sea, along the Indus and Ganges Rivers, over the Riverina of Australia, and in the northern provinces of Argentina. We have previously identified significant source areas linked to land use practices in the Sahel, Australia, east China, and the high plains of the United States, but because of weaker mean surface winds emissions are weak in these areas. There are also substantial changes in emissions rates from bare surfaces, most notably increases in SE South America, Inner Mongolia, and NE China. In North Africa, the general pattern of dust emissions is retained, but there are substantial changes in some areas, e.g., eastern Mauritania and western Mali, southeastern Algeria and western Libya, and eastern Iraq.
Table 4summarizes the emission values obtained for each continental region. Agreement is good for all regions except South Africa and South America, where M-DB2 emissions are much lower. On the other hand, there are strong regional differences in the contribution of vegetated areas, as seen inTable 4. The lowest contribution is in North Africa (4%), and the highest is in North America (78%). Globally, vegetated areas contribute 20%.
Table TABLE 4.. Annual Dust Emission (Tg yr−1) Over Eight Continental Regions (Domain Defined in Table 2) and for the Sum of the Eight Regions (Global) Using 1° × 1° Topographic Sources of Ginoux et al. (TOPO), Using M-DB2 0.1° × 0.1° Sources (M-DB2), and for M-DB2 the Contributions From Bare (BARE), Vegetated (VEGET), Nonhydrological (NHYD), Hydrological (HYD), Land Use < 30% (NAT), Land Use > 30% (ANT), Land Use < 30% and Water Bodies > 10% (NAT-H), and Land Use > 30% and Water Bodies > 10% (ANT-H) Surfaces
6.2. Emission and Hydrography
 The global distribution of dust emissions according to source type is shown in Figure 16. In Figure 16a sources associated with the ephemeral water bodies are shown in blue shading (“hydro”), and all other sources (“nonhydro”) are shown in red shading, independently of their natural or anthropogenic origin. The contribution of these two types of source (“HYD” and “NHYD”) for each region is shown in Table 4.
 Dust emission from grid cells with ephemeral water bodies represents ∼30% of global dust emission, with a maximum contribution of 71% in Australia and a minimum of 18% in North Africa. Outside North Africa, ephemeral water bodies contribute at least 25% to dust emission. The predominance of hydrological sources in Australia is linked to the absence of paleolakes with deep layers of accumulated alluvium, making them supply limited [Bullard et al., 2011]. As indicated by Prospero et al. , the most active sources in North Africa are characterized by the presence of a deep layer of sediments laid down during the Pleistocene and Holocene. In contrast, such deposits are not widely distributed in Australia, and hence, the only strong sources are dependent on the accumulation of recently deposited weathering products. It should be noted that the water body data set only captures features larger than 1 km wide; thus, it may miss a significant number of smaller lakes. This means that their contribution as shown in Table 4 should be considered as a lower limit.
6.3. Emission and Land Use
Figure 16b presents the distribution of natural (“natural,” blue shading) and anthropogenic (“anthropogenic,” red shading) sources, independently of their relation with ephemeral water bodies. The contribution of these two types (“NAT” and “ANT”) of source for each region is shown in Table 4. In addition, dust emissions from natural and anthropogenic sources from grid cells which contain more than 10% ephemeral water bodies are also provided in Table 4and are designated as “NAT-H” and “ANT-H,” respectively.
 The global annual NAT and ANT dust emissions are 1172 and 363 Tg yr−1, respectively. ANT emission represents 25% of total emission. Table 4 indicates that over North Africa ANT emission represents only 8% of African emissions, but globally, they represent 20% of anthropogenic emissions. Most anthropogenic sources in North Africa are located in the Sahel and the western Sahara. In other regions, the anthropogenic contribution to the regional emissions is much larger and varies from 30% in the Middle East and west Asia to 75% in Australia.
 The global annual NAT and ANT dust emissions, as well as their hydrologic contributions (NAT-H and ANT-H), are shown inFigure 17a. The percentage contributions of ephemeral water bodies to natural and anthropogenic emissions are shown in Figure 17b. In Australia, the hydrologic sources account for nearly 90% of the Australian anthropogenic emissions. In the Indian subcontinent, it reaches 96% because of increasing agriculture in the Indo-Gangetic floodplain. In general, anthropogenic sources related to ephemeral water bodies contribute to 85% of anthropogenic dust emission globally and regionally. The exception is South Africa with the largest contribution from nonhydrologic sources, 36%. Conversely, only 15% of natural dust sources are associated with ephemeral lakes (Table 4). North Africa accounts for 92% natural dust sources, only 11% of which are associated with ephemeral water bodies. This confirms the work of Bullard et al.  showing that about 95% of the Sahara dust plume frequency is from nonanthropogenic sources because 54% are from paleolakes.
 In the previous sections we selected a 30% threshold of land use fraction to identify anthropogenic sources and a 10 m s−1 threshold of wind erosion to calculate dust emission from anthropogenic sources. To evaluate the sensitivity of dust emissions to these two parameters, we calculated annual emissions for different values of these parameters (Table 5). As seen in Table 5, the sensitivity to land use fraction is much smaller than to the threshold of wind erosion. Indeed, reducing land use threshold from 30% to 10% increases global anthropogenic dust by 20%, while increasing it to 50% reduces the emission by 38%. On the other hand, lowering ut from 10 to 6 m s−1results in an increase of global emissions by a factor of 2–3. This is more or less true for each continental region. Thus, the threshold of wind erosion is the principal source of uncertainty in our results, and this is most likely true for all models. More robust values might be obtained by using a time-varying threshold of wind erosion which could be linked to vegetation cover and soil moisture. Another method is to use an inversion such as the one developed byDraxler et al.  to retrieve the threshold of wind erosion.
Table TABLE 5.. Annual Anthropogenic Dust Emission (Tg yr−1) Over Eight Continental Regions (Domain Defined in Table 2) and Globally, for Two Different Values of the Threshold of Wind Erosion Over Land Use Area (ut) and Three Minimum Percentages of Land Use (LU) for Attributing a Source to Anthropogenic Origins
ut = 10 m s−1
ut = 6 m s−1
LU > 10
LU > 30
LU > 50
LU > 10
LU > 30
LU > 50
 Other limitations of our work include uncertainties associated with the HIRAM wind speed and the lack of interannual variability. Due to the cubic dependency of dust emission to wind speed (cf. equation (1)), small variations in the high tail of the wind speed distribution between meteorological data sets can produce large differences in the resulting budget. Comparing HIRAM zonal winds with National Centers for Environmental Prediction (NCEP) reanalysis [Kalnay et al., 1996], Zhao et al. showed that the root-mean-square error is the lowest for HIRAM compared to 10 other models in the World Climate Research Program Coupled Model Intercomparison Project 3 database [Meehl et al., 2007]. On the other hand, Menut found a factor of 3 difference between the emission fluxes calculated with NCEP and European Centre for Medium-Range Weather Forecasts meteorological fields, NCEP having the lowest emissions. In addition to this inherent variability between models, some subscale processes important for dust generation are not explicitly resolved because of model resolution. These processes include evaporationally driven, cold, near-surface outflows from organized moist convection and turbulent circulation in dry convective boundary layer [Knippertz and Todd, 2012]. To resolve these processes explicitly, a model would require a resolution of 10 km or finer [Marsham et al., 2011], a capability not yet available for most global models. We have shown that anthropogenic sources are often located in regions influenced by monsoon winds, where such convective regimes often occur. Thus, we may underestimate dust emissions from these regions. This may also explain the apparent discrepancy between the high M-DB2 FoO sources seen in the Sahel (Figure 7) and in the southern high plains (Figure 11) but the low emissions calculated for these areas (Figure 16b).
7. RELATIONSHIP TO CLIMATE, AIR QUALITY, AND HUMAN HEALTH
 Our results indicate that up to 25% of dust is emitted from agriculture with 85% of it associated with hydrology. This implies that dust emission from these sources is particularly sensitive to land use practices and changes in the hydrological cycle. In an effort to mitigate the numerous negative effects of wind erosion, improved agricultural management practices have been developed [Ravi et al., 2011]. Projections of total agricultural land (crop plus pasture) prepared for the Intergovernmental Panel on Climate Change Fifth Assessment Report [Hurtt et al., 2011] yield a range of estimates, from a projected increase by 13% to a decrease by 24% by 2100, depending on the scenarios used. These changes are relatively small compared to expected precipitation changes. Indeed, there is a tendency for increased precipitation associated with monsoon flow but with large disparity between regions and major uncertainty in some areas [Christensen et al., 2007]. Regions that are currently dusty areas and which are likely to experience a decrease in precipitation include most of Mediterranean Europe and Africa, northern Sahara, central Asia, southwest U.S., and southern Australia in spring [Christensen et al., 2007]. Conversely, over currently dusty areas in east Africa and east Asia precipitation will likely increase [Christensen et al., 2007]. Because of large model uncertainties, projections cannot be made for the Sahel-Sudan, the Gangetic basin, and the Lake Eyre region. As a consequence of these precipitation changes we might expect a reduction in low-latitude dust sources and an intensification of sources in the tropics, unless implementation of better agricultural practices could mitigate the expected increase in dust emissions with reduced rainfall.
 Such shifts in dust sources will modulate the effects of dust on climate by changing the distribution of dust and possibly affecting its composition. Because these new agricultural dust sources areas also emit ammonia [Beusen et al., 2008] and because they are located close to fossil fuel sources of fine-mode acidic aerosols (e.g., sulfate and nitrate), dust will be increasingly mixed with such aerosols. This mixing changes the chemical and optical properties of dust, which will affect its interactions with radiation, cloud microphysics, and biogeochemical cycles. The mixing of dust with acidic species will decrease the absorption of solar radiation [Bauer et al., 2007] and yield more efficient cloud condensation nuclei, but it will decrease the formation of ice nuclei [Sullivan et al., 2010]. In addition, the presence of acidic species will increase the solubility of iron in dust particles; after deposition to the ocean, the release of iron, an essential micronutrient, can promote phytoplankton growth and consequently modulate the carbon cycle [Jickells et al., 2005]. On the other hand, it has been suggested [Mahowald et al., 2006] that natural dust loading may be reduced by 60% in a doubled carbon dioxide climate when the impacts of carbon dioxide fertilization on vegetation are included. These forcings on climate may be amplified or attenuated through positive or negative feedbacks, respectively. Miller et al.  found negative feedbacks of dust emission by dust radiative forcing through the planetary boundary layer, but Cook et al. showed that the North American “Dust Bowl” drought was amplified through human-induced land degradation. A possible desertification feedback loop by dust suppressing precipitation has been suggested [Rosenfeld et al., 2001].
 Dust, like any other aerosol, must be considered in the more general terms of its nature as particulate matter and implications for air quality. A substantial fraction of dust mass is in the “respirable” size range as defined by the U.S. Environmental Protection Agency, particles under 10 μm and under 2.5 μm diameter. Although there have been few systematic studies of the air quality impact of dust in, or proximate to, major dust source regions [De Longueville et al., 2010], it is clear that the concentrations of respirable particles in these regions can far exceed typical air quality standards [Gillies et al., 1996; Rivera Rivera et al., 2010]. Dust transported across ocean basins can have air quality impacts on receptor continents [Chin et al., 2007]. For example, African dust transported to the Caribbean [Prospero and Lamb, 2003] and Florida [Prospero et al., 2001], can rise to concentrations that challenge the U.S. air quality standard, and there is a growing recognition of the contribution of Asian dust to surface aerosol loadings in western North America [Van Curen and Cahill, 2002; Jaffe et al., 2003; Fairlie et al., 2007].
 Finally, we note that there have been relatively few studies assessing the human health impact of mineral dust as compared to other aerosols. Some investigations have evaluated health effects of dust advected from distant sources [De Longueville et al., 2010] and suggest that impacts could be substantial [Liu et al., 2009]. For example, epidemiological studies in Italy [Sajani et al., 2011] and Spain [Jiménez et al., 2010] found evidence of increased respiratory mortality among the elderly during Saharan dust events, and dust advected from mainland Asia was associated with increased risk of ischemic heart disease in Taiwan [Bell et al., 2008]. Dust transported across ocean basins can have air quality impacts on receptor continents [Chin et al., 2007]. Indeed, even in the Caribbean [Prospero and Lamb, 2003] and in Florida [Prospero et al., 2001], the concentration of African dust can rise to levels that challenge the U.S. air quality standard. Closer to the source area, dust advecting into El Paso (Texas) from the surrounding Chihuahuan Desert was found to be associated with increased odds of hospitalization for asthma and bronchitis, especially in children [Grineski et al., 2011].
 Dust storms have long been known as an exposure pathway for various fungal diseases including coccidioidomycosis [Williams et al., 1979] and aspergillosis [Chao et al., 2012]. Acute exposure to mineral dust can even, at its extreme, cause nonindustrial silicosis, recognized as “desert lung” syndrome in portions of the global dust belt [Derbyshire, 2007].
 It is clear that mineral dust can have a substantial impact on air quality and human health. Changing dust emissions with changing land use and land cover, especially where advected toward human populations, will have public policy implications with regards to compliance with air quality regulations. Consequently, it is important to develop a better understanding of the factors affecting source activity and how these might change with climate.
8. SUMMARY AND CONCLUSIONS
 The objective of this study was to develop a protocol based on the MODIS Deep Blue Level 2 (M-DB2) product that could be used to estimate the contribution of anthropogenic and hydrologic dust sources to regional and global emissions. We identified each grid cell dust source as “anthropogenic” or “hydrologic” according to the areal extent of land use and of ephemeral water bodies in each grid cell. Based on a sensitivity analysis we attributed the source to anthropogenic activities when the land use fraction was over 30%; otherwise, the source was “natural.” Each source, whether “natural” or “anthropogenic,” was further classified as either “hydrologic” when ephemeral water bodies cover over 10% of a grid cell coverage or, if less, “nonhydrologic.” We used the M-DB2 algorithm to estimate total aerosol optical depth (AOD) and dust optical depth (DOD) over arid (i.e., bright, relatively vegetation-free) regions. There was good agreement between the M-DB2 product and measurements at AERONET sites located in arid regions using data over the period 2003–2009. We found that over large regions the M-DB2 DOD often composed a major fraction of AOD.
 We next developed a global seasonal picture of the most active dust source regions at 0.1° resolution based on the distribution of the frequency of occurrence (FoO) of DOD > 0.2. The M-DB2 product shows that the most active dust sources are located in a broad band that extends from the west coast of North Africa through the Middle East to central Asia. In contrast, there is remarkably little dust activity in the Southern Hemisphere. The M-DB2 distribution was compared to distributions derived previously using the Nimbus 7 TOMS aerosol index based on data from 1978 to 1991 [Prospero et al., 2002] and also with the more recent OMI aerosol index which covers 2003 to 2006. These three data sets yield similar dust distributions over North Africa, the Middle East, and South America, thereby indicating that there have been no major changes in dust activity over these regions over 3 decades. In contrast, we found substantial changes in the U.S. high plains, central Asia, and Australia.
 An analysis of source attributions over different continental regions reveals consistent patterns and relationships. In North Africa, anthropogenic and hydrologic sources are mostly located within river basins in the Sahel and also along the Mediterranean coast. We also observed small but significant anthropogenic sources in southern Spain and Turkey. In Asia, major dust sources are linked to the Aral Sea, Lake Balkhash, and Urumia Lake, all of which have been desiccated as a result of water diversion. In the Middle East, the largest anthropogenic sources are observed in Mesopotamia and Saudi Arabia. Anthropogenic sources were dominant across the entire Gangetic Basin during the premonsoon. In China, large anthropogenic sources are found in the Horqin sandy region and in the north China plains. Some of these sources are in extensively industrialized areas. In South America Patagonia is a major anthropogenic source largely linked to livestock grazing. Major river basins are clearly apparent as dust sources in Mesopotamia, the Indo-Gangetic basin, North America, and Australia. A particularly good example of M-DB2 sensitivity is the detection of dust along the entire length of the Darling River in Australia whose course is made visible (Figure 14) as a long narrow dust source. Severe droughts appear to be the cause of some of the observed source activities. In North America dust sources are observed in most of the high plains. In South Africa, we found anthropogenic sources north of Cape Town and Bloemhof reservoir. We found several sources of dust in southern Madagascar, which are most likely linked to intense deforestation followed by erosion.
 Finally, we calculated emissions from these sources using a high-resolution data set of wind speed for the year 2005. The global annual emissions are 1536 Tg yr−1, which corresponds well to the mean value of multimodel comparison [Huneeus et al., 2011]. We found that 20% of total emissions are from vegetated areas. These areas include the Sahel, Kazakhstan, Indo-Gangetic basin, east China, several states of Australia, Argentina, and the U.S. high plains.
 We found that 30% of global dust emission originates from terrains associated with ephemeral water bodies. In West Africa, they account for only 18% of regional emissions, while in all other regions they contribute over twice as much. These percentages might have been even larger had we been able to include hydrological features smaller than 1 km (e.g., ephemeral streams, small lakes, and ponds). It is notable that in Australia ephemeral water sources, natural and anthropogenic, make the largest contribution to total emissions, 71%.
 Although we found widespread examples of anthropogenic sources, they account for only 25% of global dust emissions. The reason is that North Africa contributes 55% of global emissions but only 8% to global anthropogenic emissions. In other regions, the percentages of anthropogenic emissions are much higher but have a small impact on global budgets. For example, Australia with 75% anthropogenic dust accounts for only 13% of the global anthropogenic emissions. About 85% of all anthropogenic emissions are associated with ephemeral water bodies. This relationship might be linked to the use of water resources for croplands, for urban use, and for grazing ranges for sheep and cattle. It also implies that because of this association, the activity of these sources could change greatly with changing climate. On the other hand, natural sources are weakly related to ephemeral water bodies with only 15% associated with presently ephemeral water bodies. This can be explained by the important role that paleolakes play as sources of aeolian dust.
 Our methodology based on M-DB2 is the first that enables us to estimate DOD. Because of the high resolution, we can more closely relate our product to land use and other features. This enables us for the first time to estimate emissions in a more systematic and quantitative way and, in particular, to characterize emissions from anthropogenic sources. The major source of uncertainty in the calculation of emissions is due to the uncertainties in the threshold of wind erosion. To reduce this uncertainty, it will be necessary to have a better estimate of these threshold velocities for different terrain conditions and to include the time varying dependency of the threshold on vegetation cover and soil moisture. This might be accomplished using satellite data sets or using values derived by the inversion technique developed byDraxler et al. . In addition, the model used in this study could not resolve some subgrid-scale dynamical processes that could produce haboobs, downbursts, and dust devils. In the few cases were they have been simulated, they appear to generate significant dust loading, particularly in areas with anthropogenic sources. However, global model resolution continually improves, so we can expect that in the near future we will be able to evaluate their importance at the subcontinental and global scales.
 As stated above, we found that a large fraction of emissions, at least 30%, is related to the hydrological cycle. This association could be a source of strong interannual variability. To better address this issue, longer data records should be used. The 14 year record of aerosol products from the SeaWiFS instrument could be useful after detailed comparison of the dust inventories derived from the different satellite instruments with geomorphologic characterization such as that derived by Bullard et al. .
 Projected precipitation changes with changing climate may increase dust emission from tropical dust sources at the expense of low-latitude and midlatitude sources. However, the projections of precipitation changes are highly uncertain in some regions (e.g., sub-Saharan Africa) which are known to be highly active sources today. Consequently, it is difficult to anticipate how dust source locations might change and how these changes might impact emissions. Nonetheless, any shifts in dust source location and emission will modify the effects of dust on climate. As a significant fraction of these subtropical sources are associated with agriculture, the coemission of ammonia and the proximity of fine-mode acidic aerosols (e.g., sulfate) from fossil fuel burning will increase their internal mixing with dust. Such mixing would change the chemical and optical properties of dust which, in turn, would affect its lifetime and the interactions with radiation, cloud microphysics, and biogeochemical cycles. While it is difficult to anticipate in detail such changes, it is clear that there is a highly complex linkage between climate, human activities, and dust emissions and that we need a better quantitative understanding of those relationships before we can assess possible feedbacks on climate, air quality, and public health. In presenting our results we focused for the most part on major dust sources and examples that illustrated various aspects of dust mobilization on a global scale. However, we hope that our results will stimulate research on specific dust source areas. For this purpose, the data presented inFigures 7–14 can be visualized with ultrahigh resolution on Google Earth by downloading files (KML or compressed KMZ format) from http://www.gfdl.noaa.gov/atmospheric-physics-and-chemistry_data. KML versions of Figures 7–14 are available in the auxiliary material.
 The authors thank the AERONET program for establishing and maintaining the Sun photometer sites used in this study. We are grateful to the NASA TOMS and OMI science teams for providing the aerosol index. We are grateful to Catherine Raphael for helping with the figures. T. E. Gill acknowledges support via NOAA cooperative agreement NA17AE1623, and J. M. Prospero was supported by grants from the U.S. National Science Foundation, OCE 0623189 and AGS 0962256.
 The Editor of this paper was Greg Okin. He thanks four anonymous reviewers.