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circulation and/or frontal boundary. Instead, they consist of multiple local/regional storms that form along the advancing dust haze itself or as the result of global teleconnections associated with the high loading of dust ( Strausberg et al. 2005 ; Cantor 2007 ). Regional dust storms can form from merging local storms but are often associated with discrete weather systems, particularly fronts ( Cantor et al. 2001 ; Cantor 2007 ; Wang and Richardson 2015 ). Global storms loft dust up to 75 km above
circulation and/or frontal boundary. Instead, they consist of multiple local/regional storms that form along the advancing dust haze itself or as the result of global teleconnections associated with the high loading of dust ( Strausberg et al. 2005 ; Cantor 2007 ). Regional dust storms can form from merging local storms but are often associated with discrete weather systems, particularly fronts ( Cantor et al. 2001 ; Cantor 2007 ; Wang and Richardson 2015 ). Global storms loft dust up to 75 km above
and interpretation of long-term trends and variability. Consistent with World Meteorological Organization (WMO) guidelines ( WMO 2009 ), the present-weather record in DS-3505 includes 11 dust categories ( Table 1 ). During the study period, there were 916 reports of blowing dust (category 7), 178 of dust in suspension (category 6), 7 of dust storm (categories 9, 30–32, and 98), and 1 of dust or sand whirl (category 8) at KSLC. There were no reports of severe dust storm (categories 33–35). Among
and interpretation of long-term trends and variability. Consistent with World Meteorological Organization (WMO) guidelines ( WMO 2009 ), the present-weather record in DS-3505 includes 11 dust categories ( Table 1 ). During the study period, there were 916 reports of blowing dust (category 7), 178 of dust in suspension (category 6), 7 of dust storm (categories 9, 30–32, and 98), and 1 of dust or sand whirl (category 8) at KSLC. There were no reports of severe dust storm (categories 33–35). Among
that time there has been a steady increase in the number of publications related to dust outbreaks ( Stout et al. 2009 ), and since the dawn of the satellite era the rate of publications on Saharan dust has grown exponentially ( Kaufman et al. 2005b ). One interesting subset of study into aeolian dust focuses on the relationship between climate variability and African dust outbreaks. Much focus has been placed on demonstrating that Atlantic dust storm frequency and intensity changes are forced by
that time there has been a steady increase in the number of publications related to dust outbreaks ( Stout et al. 2009 ), and since the dawn of the satellite era the rate of publications on Saharan dust has grown exponentially ( Kaufman et al. 2005b ). One interesting subset of study into aeolian dust focuses on the relationship between climate variability and African dust outbreaks. Much focus has been placed on demonstrating that Atlantic dust storm frequency and intensity changes are forced by
convection that mixes dust and water vapor into the middle atmosphere, which is called dusty deep convection (DDC) in line with the deeply penetrating convection simulated by Spiga et al. (2013) . DDC was first suspected by Gierasch and Goody (1973) , who proposed Martian dust storms might resemble hurricanes and thus have deeply mixed dust concentrated near their centers with vertical velocities on the order of 0.1 m s −1 . Furthermore, plume-like, cumuliform, and/or cellular organization of dust
convection that mixes dust and water vapor into the middle atmosphere, which is called dusty deep convection (DDC) in line with the deeply penetrating convection simulated by Spiga et al. (2013) . DDC was first suspected by Gierasch and Goody (1973) , who proposed Martian dust storms might resemble hurricanes and thus have deeply mixed dust concentrated near their centers with vertical velocities on the order of 0.1 m s −1 . Furthermore, plume-like, cumuliform, and/or cellular organization of dust
those associated with the cold pools produced by convective storms, are a public safety hazard due to rapid losses in visibility ( Baddock et al. 2013 ; Sprigg 2016 ; Middleton and Kang 2017 ) and damages to human respiratory health ( Goudie 2014 ; Middleton 2017 ). Haboobs are dust storms that occur as a result of the lofting of dust by the strong lateral winds originating within cold pools. Cold pools are a type of density current and form as precipitation evaporates in dry air below the
those associated with the cold pools produced by convective storms, are a public safety hazard due to rapid losses in visibility ( Baddock et al. 2013 ; Sprigg 2016 ; Middleton and Kang 2017 ) and damages to human respiratory health ( Goudie 2014 ; Middleton 2017 ). Haboobs are dust storms that occur as a result of the lofting of dust by the strong lateral winds originating within cold pools. Cold pools are a type of density current and form as precipitation evaporates in dry air below the
patterns of dust storms are also documented by Rezazadeh et al. (2013) using visibility records for the period 1998–2003. Utilizing the Total Ozone Mapping Spectrometer (TOMS)–derived aerosol index (AI), for a 14.5-yr period (1978–93), the maximum of dust storm activity is identified over eastern and central Saudi Arabia (Ad Dahna Desert) as well as the Saudi–Oman border (Rub al Khali or Empty Quarter Desert) during the summer months ( Washington et al. 2003 ). Prospero et al. (2002) , also using
patterns of dust storms are also documented by Rezazadeh et al. (2013) using visibility records for the period 1998–2003. Utilizing the Total Ozone Mapping Spectrometer (TOMS)–derived aerosol index (AI), for a 14.5-yr period (1978–93), the maximum of dust storm activity is identified over eastern and central Saudi Arabia (Ad Dahna Desert) as well as the Saudi–Oman border (Rub al Khali or Empty Quarter Desert) during the summer months ( Washington et al. 2003 ). Prospero et al. (2002) , also using
1. Introduction Dust storms are a disastrous weather type. They arise in desert areas and release substantial amounts of aerosolized dust into the atmosphere ( Engelstaedter et al. 2006 ; Boucher et al. 2013 ). This airborne dust can reduce visibility and air quality and cause respiratory and circulatory system diseases ( Degobbi et al. 2011 ). Dust particles can be transported on regional or global scales ( Shao and Dong 2006 ), directly or indirectly transforming atmospheric systems. This
1. Introduction Dust storms are a disastrous weather type. They arise in desert areas and release substantial amounts of aerosolized dust into the atmosphere ( Engelstaedter et al. 2006 ; Boucher et al. 2013 ). This airborne dust can reduce visibility and air quality and cause respiratory and circulatory system diseases ( Degobbi et al. 2011 ). Dust particles can be transported on regional or global scales ( Shao and Dong 2006 ), directly or indirectly transforming atmospheric systems. This
rainfall by changing the atmospheric heating profile and hence the moisture convergence ( Lau et al. 2006 ; Vinoj et al. 2014 ; Jin et al. 2014 ; Solmon et al. 2015 ; Kim et al. 2016 ). Understanding these mechanisms and the way they influence the Indian summer monsoon is critical for South Asia since the region depends, directly or indirectly, on the monsoon rainfall. Most of the studies on dust transport over the northern IO have focused on the Indo-Gangetic Plain (IGP; e.g., Dey et al. 2004
rainfall by changing the atmospheric heating profile and hence the moisture convergence ( Lau et al. 2006 ; Vinoj et al. 2014 ; Jin et al. 2014 ; Solmon et al. 2015 ; Kim et al. 2016 ). Understanding these mechanisms and the way they influence the Indian summer monsoon is critical for South Asia since the region depends, directly or indirectly, on the monsoon rainfall. Most of the studies on dust transport over the northern IO have focused on the Indo-Gangetic Plain (IGP; e.g., Dey et al. 2004
days, SST is a function of wind speed. While strong surface winds are expected in the presence of an AEW or TC, storm-forced SST cooling ( Price 1981 ; Sanford et al. 1987 ) can weaken the parent ( Black and Holland 1995 ) and the future storms ( Brand 1971 ). In our simulations, we use ECMWF operational analysis, which has assimilated observational data and contains both SST and winds, as our initial and boundary conditions. The model calculates the meteorological fields within the domain
days, SST is a function of wind speed. While strong surface winds are expected in the presence of an AEW or TC, storm-forced SST cooling ( Price 1981 ; Sanford et al. 1987 ) can weaken the parent ( Black and Holland 1995 ) and the future storms ( Brand 1971 ). In our simulations, we use ECMWF operational analysis, which has assimilated observational data and contains both SST and winds, as our initial and boundary conditions. The model calculates the meteorological fields within the domain
XMET—An Unattended Meteorological Sensing System for Austere Environmentsengulfed stations XM1 and XM2, corresponding to visibility observations near zero, while good visibility conditions were observed to the north. OA maps derived from the XMET array captured some of the patchiness in the eastern side of the dust plume delineating potential go–no go regions for ground or aviation operations. The analysis suggests that additional XMETs deployed further upstream, closer to the source dust regions, could improve forecasts of dust storms at the southern XMET sites. 2) Typhoon
engulfed stations XM1 and XM2, corresponding to visibility observations near zero, while good visibility conditions were observed to the north. OA maps derived from the XMET array captured some of the patchiness in the eastern side of the dust plume delineating potential go–no go regions for ground or aviation operations. The analysis suggests that additional XMETs deployed further upstream, closer to the source dust regions, could improve forecasts of dust storms at the southern XMET sites. 2) Typhoon
