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Global and Continental Drought in the Second Half of the Twentieth Century: Severity–Area–Duration Analysis and Temporal Variability of Large-Scale Events

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Global and Continental Drought in the Second Half of the Twentieth Century: Severity–Area–Duration Analysis and Temporal Variability of Large-Scale Events 1962 JOURNAL OF CLIMATE VOLUME 22 Global and Continental Drought in the Second Half of the Twentieth Century: Severity–Area–Duration Analysis and Temporal Variability of Large-Scale Events J. SHEFFIELD Department of Civil and Environmental Engineering, Princeton University, Princeton, New Jersey K. M. ANDREADIS Department of Civil and Environmental Engineering, University of Washington, Seattle, Washington E. F. WOOD Department of Civil and Environmental Engineering, Princeton University, Princeton, New Jersey D. P. LETTENMAIER Department of Civil and Environmental Engineering, University of Washington, Seattle, Washington (Manuscript received 10 July 2008, in final form 15 October 2008) ABSTRACT Using observation-driven simulations of global terrestrial hydrology and a cluster algorithm that searches for spatially connected regions of soil moisture, the authors identified 296 large-scale drought events (greater than 500 000 km2 and longer than 3 months) globally for 1950–2000. The drought events were subjected to a severity–area–duration (SAD) analysis to identify and characterize the most severe events for each continent and globally at various durations and spatial extents. An analysis of the variation of large-scale drought with SSTs revealed connections at interannual and possibly decadal time scales. Three metrics of large-scale drought (global average soil moisture, contiguous area in drought, and number of drought events shorter than 2 years) are shown to covary with ENSO SST anomalies. At longer time scales, the number of 12-month and longer duration droughts follows the smoothed variation in northern Pacific and Atlantic SSTs. Globally, the mid-1950s showed the highest drought activity and the mid-1970s to mid-1980s the lowest activity. This physically based and probabilistic approach confirms well-known droughts, such as the 1980s in the Sahel region of Africa, but also reveals many severe droughts (e.g., at high latitudes and early in the time period) that have received relatively little attention in the scientific and popular literature. 1. Introduction mosphere and feedbacks with the oceans and land sur- face (e.g., Jiang et al. 2006; McCabe and Palecki 2006). Drought is a naturally occurring climate phenomenon These are modulated by external forcings such as vari- that impacts human and environmental activity glob- ations in solar input and atmospheric composition, ei- ally. It is among the costliest and most widespread of ther natural or anthropogenic. natural disasters (Wilhite 2000). One of the reasons for The scientific body of research into the processes that this is the usually large spatial extent of droughts and cause drought to develop and persist is growing rapidly. their lengthy duration, sometimes reaching continental This research has highlighted a number of factors that scales and lasting for many years. Drought is generally may potentially impact drought occurrence including driven by extremes in the natural variation of climate, large-scale atmospheric mechanisms that are associated which are forced by the internal interactions of the at- with modes of climate variability and sea surface tem- perature (SST) anomalies (Schubert et al. 2004; Seager Corresponding author address: Justin Sheffield, Department of Civil and Environmental Engineering, Princeton University, et al. 2005), and evidence that land–atmosphere feed- Princeton, NJ 08544. backs play a role in their persistence (Long et al. 2000; E-mail: [email protected] Wang and Eltahir 2000). DOI: 10.1175/2008JCLI2722.1 Ó 2009 American Meteorological Society Unauthenticated | Downloaded 10/06/21 05:11 PM UTC 15 APRIL 2009 S H E F F I E L D E T A L . 1963 However, much of this research is based on coupled because it provides an aggregate estimate of available land–atmosphere–ocean models, and may be model spe- water from the balance of precipitation, evaporation, cific. Part of the reason that the research has favored and runoff fluxes. It also reflects the delays in the hy- model-based approaches, and for our general lack of drologic system caused by infiltration, drainage, snow understanding of the mechanisms that control drought accumulation and melt, and the impacts of variation and development and persistence, is the dearth of detailed anomalies in the meteorological drivers (such as changes observational data of the occurrence and variability of in storm frequency and intensity). In drought termi- droughts over large time and space scales. Alterna- nology it most closely represents agricultural drought tively, land surface models forced by surface climate through its control on transpiration and thus plant observations (which generally are more available than growth, but reflects meteorological and hydrological the relevant terrestrial hydrologic variables) can pro- drought because of the intimate links through the land- vide spatially and temporally consistent derived fields of surface water balance. variables that are not observed directly (Mitchell et al. We calculate an index of drought as the deficit of soil 2004; Sheffield and Wood 2007; Wang et al. 2009). They moisture relative to its seasonal climatology at a loca- can also form the basis for seasonal hydrologic predic- tion (Sheffield et al. 2004a). This allows us to compare tion (Wood and Lettenmaier 2006) and thus drought the occurrence of drought between different locations forecasting (Luo and Wood 2007). in a consistent and meaningful way. Daily soil moisture The Palmer drought severity index (PDSI) (Palmer data output from the VIC model are averaged to a monthly 1965) has generally been the tool of choice for observation- time step and transformed to percentiles. A drought is based indices of drought, and has been used by Cook then defined conceptually as a sequence of spatially et al. (1999) and Dai et al. (2004b), among others, for contiguous deficits below the 20th percentile, which drought reconstruction. However, the PDSI has notable represents relatively rare conditions. This value has deficiencies, including its inability to represent the ef- been used in a previous application to the United States fects of snow and the absence of a sound probabilistic (A05) and is in line with drought thresholds used by the interpretation for the resulting index values. An alter- U.S. Drought Monitor (National Drought Mitigation native to the PDSI is the use of land surface models that Center 2003). In semiarid and arid regions, it should be simulate the detailed processes of water and energy noted that absolute soil moisture values are generally transfer at the earth’s surface (see e.g., Sheffield et al. low and drought can be considered to be the norm in 2004a; Andreadis et al. 2005, hereafter A05). terms of available water. The 20th percentile threshold This study follows this approach and builds on pre- therefore represents very dry values in these regions, and vious work into the occurrence and trends in drought our definition of drought should be regarded as con- during the twentieth century over the United States ceptual rather than physical. We summarize below the (Sheffield et al. 2004a; A05; Andreadis and Lettenmaier hydrologic simulation and the methods for drought 2006) and globally (Sheffield and Wood 2007, 2008). We identification and analysis. For more details, the reader is analyze derived soil moisture from simulations of the referred to Sheffield and Wood (2007) and A05. terrestrial hydrologic cycle using the Variable Infiltra- a. Variable Infiltration Capacity global hydrologic tion Capacity (VIC) model to quantify the global oc- simulation currence of drought for 1950–2000. Using the severity– area–duration (SAD) analysis methods of A05 we The VIC model (Liang et al. 1994; Cherkauer et al. identify major drought events and explore their spa- 2002) simulates the land-surface water and energy bal- tiotemporal characteristics and relationships with large- ances and has been used extensively for modeling scale climate variability. studies at regional (Maurer et al. 2002; Su et al. 2006) to global scales (Nijssen et al. 2001; Sheffield et al. 2004b) and regional climate change impact assessment (Hamlet 2. Datasets and methods and Lettenmaier 1999; Hayhoe et al. 2007). The simu- Soil moisture fields are taken from observation-driven lations were run for 1950–2000 at 1.08 resolution over simulations of the terrestrial hydrologic cycle using the global land areas except Greenland and Antarctica. VIC model [although the VIC model is our choice ow- They were driven by a hybrid observation–reanalysis ing to its heritage as outlined above, Wang et al. (2009) meteorological dataset (Sheffield et al. 2006) that com- show that comparable results can be achieved using bines gridded observations of precipitation, tempera- alternative land surface models and, in any event, the ture, and radiation with data from the National Centers methods described here are not specific to the VIC for Environmental Prediction–National Center for Atmo- model]. Soil moisture is a useful indicator of drought spheric Research (NCEP–NCAR) reanalysis (Kalnay et al. Unauthenticated | Downloaded 10/06/21 05:11 PM UTC 1964 JOURNAL OF CLIMATE VOLUME 22 1996) to produce a high-resolution and bias-corrected corresponding to the storm centers of the DAD analysis forcing dataset. The simulations are described in detail (WMO 1969). The block neighborhood of the center is in Sheffield and Wood (2007) and have been validated then searched for the next largest severity and that pixel against available terrestrial hydrologic observations
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