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^ and −∇ H p point in the same direction, such that t ^ is orthogonal to ∇ H p and D H V / Dt vanishes. In purely unbalanced flow (i.e., flow that is accelerating directly with the pressure gradient force), t ^ and −∇ H p point in the same direction and the radius of curvature R vanishes. Thus, the angle ϕ = cos − 1 [ − ( ∇ H p ⋅ n ^ / | ∇ H p | ) ] between n ^ and −∇ H p measures the degree to which air parcel motions are cyclostrophically balanced, with ϕ = 0 implying an
^ and −∇ H p point in the same direction, such that t ^ is orthogonal to ∇ H p and D H V / Dt vanishes. In purely unbalanced flow (i.e., flow that is accelerating directly with the pressure gradient force), t ^ and −∇ H p point in the same direction and the radius of curvature R vanishes. Thus, the angle ϕ = cos − 1 [ − ( ∇ H p ⋅ n ^ / | ∇ H p | ) ] between n ^ and −∇ H p measures the degree to which air parcel motions are cyclostrophically balanced, with ϕ = 0 implying an
where the amplitude of the anomalies exceeds two standard deviations. The substantial differences in the record heat and drought that developed over the United States during 2011 and 2012 offer an important opportunity to assess further the differing roles of SST forcing in the development of such extreme events. The 2011 and 2012 U.S. droughts were accompanied by SST anomalies that had important similarities as well as some differences. Figure 2 shows that La Niña conditions existed in the
where the amplitude of the anomalies exceeds two standard deviations. The substantial differences in the record heat and drought that developed over the United States during 2011 and 2012 offer an important opportunity to assess further the differing roles of SST forcing in the development of such extreme events. The 2011 and 2012 U.S. droughts were accompanied by SST anomalies that had important similarities as well as some differences. Figure 2 shows that La Niña conditions existed in the
impact is much larger in the developing world, where agriculture typically occupies a larger percentage of the labor force and food insecurity is a major concern ( Brown and Funk 2008 ). Given the magnitude of projected changes in drought from climate models ( Dai 2011 ), the potential increase in susceptibility to droughts is alarming. Even though Sheffield et al. (2012) found little evidence indicating a change in the occurrence of drought events globally over the past 60 years, the
impact is much larger in the developing world, where agriculture typically occupies a larger percentage of the labor force and food insecurity is a major concern ( Brown and Funk 2008 ). Given the magnitude of projected changes in drought from climate models ( Dai 2011 ), the potential increase in susceptibility to droughts is alarming. Even though Sheffield et al. (2012) found little evidence indicating a change in the occurrence of drought events globally over the past 60 years, the
NOAA’s Climate Program Office, which set up a Drought Task Force (DTF) with the overarching goal of advancing drought understanding, monitoring, and prediction through coordinated research activities that address a number of NIDIS-relevant scientific objectives. These include (i) the scientific understanding of the weather and climatic mechanisms that lead to the onset, maintenance, and recovery of drought; (ii) improving drought prediction skill by identifying and exploiting sources of drought
NOAA’s Climate Program Office, which set up a Drought Task Force (DTF) with the overarching goal of advancing drought understanding, monitoring, and prediction through coordinated research activities that address a number of NIDIS-relevant scientific objectives. These include (i) the scientific understanding of the weather and climatic mechanisms that lead to the onset, maintenance, and recovery of drought; (ii) improving drought prediction skill by identifying and exploiting sources of drought
subtropics and a poleward expansion of subtropical dry zones ( Solomon et al. (2007) ; Seager et al. 2010b ; Cayan et al. 2010 ) and also a shift to more extreme precipitation events. Was the TexMex drought a case of such anthropogenically induced climate change? It would certainly be rash to draw such a conclusion given that past droughts in the U.S. Southwest and Plains have been reliably attributed to forcing of atmospheric circulation anomalies by naturally occurring cool tropical Pacific and, to a
subtropics and a poleward expansion of subtropical dry zones ( Solomon et al. (2007) ; Seager et al. 2010b ; Cayan et al. 2010 ) and also a shift to more extreme precipitation events. Was the TexMex drought a case of such anthropogenically induced climate change? It would certainly be rash to draw such a conclusion given that past droughts in the U.S. Southwest and Plains have been reliably attributed to forcing of atmospheric circulation anomalies by naturally occurring cool tropical Pacific and, to a
the majority of precipitation falls in July and August. Both of these mechanisms were largely absent or inoperative to a considerable degree in 2012 over the central Great Plains. Diagnosis of 500-hPa height anomalies during summer 2012 reveals considerable monthly variability ( Fig. 5 ), implying that the drought was not a consequence of some steady sustained forcing. Yet each of these monthly anomaly patterns in their own manner squelched rainfall-inducing processes over the central plains. In
the majority of precipitation falls in July and August. Both of these mechanisms were largely absent or inoperative to a considerable degree in 2012 over the central Great Plains. Diagnosis of 500-hPa height anomalies during summer 2012 reveals considerable monthly variability ( Fig. 5 ), implying that the drought was not a consequence of some steady sustained forcing. Yet each of these monthly anomaly patterns in their own manner squelched rainfall-inducing processes over the central plains. In
part because of variations among multiple drought indicators, different land surface models, and forcings. Mo et al. (2012) compared the NCEP and UW products, which use different land surface models and forcing data. They found that the SM and runoff differences between systems are larger over the western than the eastern United States, and in general, the differences were too large to support drought classification. The differences between the two sets of products were mostly attributable to
part because of variations among multiple drought indicators, different land surface models, and forcings. Mo et al. (2012) compared the NCEP and UW products, which use different land surface models and forcing data. They found that the SM and runoff differences between systems are larger over the western than the eastern United States, and in general, the differences were too large to support drought classification. The differences between the two sets of products were mostly attributable to
evaluated drought forecast skill using a set of hindcast experiments ( Mo et al. 2012 ; Yoon et al. 2012 ; Yuan et al. 2013 ). The CGCM-based drought forecasting approach can be divided in two steps. First, meteorological forcings from the CGCM forecasts are bias corrected and downscaled to the resolution that is suitable for regional applications, with the resulting precipitation used to calculate a meteorological drought index, such as the Standardized Precipitation Index (SPI; McKee et al. 1993
evaluated drought forecast skill using a set of hindcast experiments ( Mo et al. 2012 ; Yoon et al. 2012 ; Yuan et al. 2013 ). The CGCM-based drought forecasting approach can be divided in two steps. First, meteorological forcings from the CGCM forecasts are bias corrected and downscaled to the resolution that is suitable for regional applications, with the resulting precipitation used to calculate a meteorological drought index, such as the Standardized Precipitation Index (SPI; McKee et al. 1993
records extend through 2005. The USHCN stations are located in relatively flat regions scattered across the CONUS and feature a mean elevation of about 520 m ( Fig. 1 ). c. NLDAS forcing The NLDAS project has produced over 30 years of retrospective and real-time forcing from 1979 to the present to support its land surface modeling activities ( Cosgrove et al. 2003 ; Xia et al. 2012 ). NLDAS forcing features a ⅛° spatial resolution and an hourly temporal resolution and is based on spatially and
records extend through 2005. The USHCN stations are located in relatively flat regions scattered across the CONUS and feature a mean elevation of about 520 m ( Fig. 1 ). c. NLDAS forcing The NLDAS project has produced over 30 years of retrospective and real-time forcing from 1979 to the present to support its land surface modeling activities ( Cosgrove et al. 2003 ; Xia et al. 2012 ). NLDAS forcing features a ⅛° spatial resolution and an hourly temporal resolution and is based on spatially and
monthly anomalies and percentiles of hydrologic fields (soil moisture, snow water equivalent, total runoff, streamflow, evaporation, and precipitation) output from the four land surface models [Noah, Mosaic, Sacramento (SAC), and Variable Infiltration Capacity (VIC)] on a common ⅛° grid using common hourly meteorological forcing (see the drought tab on the NLDAS website, www.emc.ncep.noaa.gov/mmb/nldas ). The climatology of each hydrologic field was calculated as the average of 28 yr (1980–2007) of
monthly anomalies and percentiles of hydrologic fields (soil moisture, snow water equivalent, total runoff, streamflow, evaporation, and precipitation) output from the four land surface models [Noah, Mosaic, Sacramento (SAC), and Variable Infiltration Capacity (VIC)] on a common ⅛° grid using common hourly meteorological forcing (see the drought tab on the NLDAS website, www.emc.ncep.noaa.gov/mmb/nldas ). The climatology of each hydrologic field was calculated as the average of 28 yr (1980–2007) of
