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Primary Atmospheric Drivers of Pluvial Years in the United States Great Plains University of Nebraska - Lincoln DigitalCommons@University of Nebraska - Lincoln HPRCC Personnel Publications High Plains Regional Climate Center 4-2018 Primary Atmospheric Drivers of Pluvial Years in the United States Great Plains Paul Flanagan Jeffrey B. Basara Jason C. Furtado Xiangming Xiao Follow this and additional works at: https://digitalcommons.unl.edu/hprccpubs Part of the Atmospheric Sciences Commons, Climate Commons, Environmental Indicators and Impact Assessment Commons, Environmental Monitoring Commons, Fresh Water Studies Commons, Hydrology Commons, Meteorology Commons, Natural Resources Management and Policy Commons, Sustainability Commons, and the Water Resource Management Commons This Article is brought to you for free and open access by the High Plains Regional Climate Center at DigitalCommons@University of Nebraska - Lincoln. It has been accepted for inclusion in HPRCC Personnel Publications by an authorized administrator of DigitalCommons@University of Nebraska - Lincoln. APRIL 2018 F L A N AGAN ET AL. 643 Primary Atmospheric Drivers of Pluvial Years in the United States Great Plains PAUL X. FLANAGAN School of Meteorology, University of Oklahoma, Norman, Oklahoma JEFFREY B. BASARA School of Meteorology, and Oklahoma Climatological Survey, University of Oklahoma, Norman, Oklahoma JASON C. FURTADO School of Meteorology, University of Oklahoma, Norman, Oklahoma XIANGMING XIAO Department of Microbiology and Plant Biology, and Center for Spatial Analysis, University of Oklahoma, Norman, Oklahoma (Manuscript received 2 August 2017, in final form 26 February 2018) ABSTRACT Precipitation variability has increased in recent decades across the Great Plains (GP) of the United States. Drought and its associated drivers have been studied in the GP region; however, periods of excessive pre- cipitation (pluvials) at seasonal to interannual scales have received less attention. This study narrows this knowledge gap with the overall goal of understanding GP precipitation variability during pluvial periods. Through composites of relevant atmospheric variables from the ECMWF twentieth-century reanalysis (ERA-20C), key differences between southern Great Plains (SGP) and northern Great Plains (NGP) pluvial periods are highlighted. The SGP pluvial pattern shows an area of negative height anomalies over the southwestern United States with wind anomalies consistent with frequent synoptic wave passages along a southward-shifted North Pacific jet. The NGP pattern during pluvial periods, by contrast, depicts anomalously low heights in the northwestern United States and an anomalously extended Pacific jet. Analysis of daily heavy precipitation events reveals the key drivers for these pluvial events, namely, an east–west height gradient and associated stronger poleward moisture fluxes. Therefore, the results show that pluvial years over the GP are likely driven by synoptic-scale processes rather than by anomalous seasonal precipitation driven by longer time-scale features. Overall, the results present a possible pathway to predicting the occurrence of pluvial years over the GP and understanding the causes of GP precipitation variability, potentially mitigating the threats of water scarcity and excesses for the public and agricultural sectors. 1. Introduction temperatures are climatologically at their maximum, the water stress on crops and the surface is dramatically Precipitation is a critical asset for extensive agricul- increased. While irrigation can offset the impact of this ture across the Great Plains (GP) of the United States water stress, conditions that bring about precipitation (Fischer et al. 2007). The GP of the United States deficits typically cause abnormal temperature patterns, (herein defined as the states of Texas, Oklahoma, and further crop damage can still occur (e.g., Wilhite Kansas, Nebraska, South Dakota, and North Dakota) 2000; Wilhelmi and Wilhite 2002; Hoerling et al. 2014; possesses a unique precipitation climatology in that the Yin et al. 2014; Livneh and Hoerling 2016). Thus, pre- climatological maxima of rainfall and temperature are cipitation deficits and excesses are critically important asynchronous and occur at different times of the plant- for the GP. growing season (Flanagan et al. 2017). Thus, if a pre- The GP is also a region of high precipitation vari- cipitation deficit occurs during the time of year in which ability across multiple spatial and temporal scales (e.g., Ting and Wang 1997; Ruiz-Barradas and Nigam 2005; Corresponding author: Paul Flanagan, [email protected] Flanagan et al. 2017). Droughts occur with enough DOI: 10.1175/JHM-D-17-0148.1 Ó 2018 American Meteorological Society. For information regarding reuse of this content and general copyright information, consult the AMS Copyright Policy (www.ametsoc.org/PUBSReuseLicenses). 644 JOURNAL OF HYDROMETEOROLOGY VOLUME 19 frequency that numerous studies have investigated the and a more comprehensive analysis of many events drivers of such events within the GP region (Basara et al. spanning multiple decades remains to be done. 2013). A majority of these studies focused on the con- The objective of our study is to use long-period (i.e., nections between various sea surface temperature (SST) spanning the twentieth and twenty-first centuries) cli- patterns and their influence on anomalous synoptic matological reanalysis datasets to examine past pluvial flow patterns and consequently GP precipitation (e.g., periods in the GP of the United States and describe Trenberth and Branstator 1992; Schubert et al. 2004; qualitatively and quantitatively the primary atmo- Seager et al. 2005; Cook et al. 2008; Seager and Hoerling spheric drivers of such events. Along with filling a gap in 2014). Aside from SST patterns, other forcing mecha- the climate literature, this work will also contribute to nisms contributing to drought in the GP region include emerging studies on the changing nature of GP pre- internal atmospheric variability (Seager et al. 2014) and cipitation both in the recent past (e.g., Christian et al. land–atmosphere coupling (Mo et al. 1997; Koster et al. 2015; Weaver et al. 2016; Flanagan et al. 2017) and under 2000; Schubert et al. 2004). future climate change (e.g., Rosenzweig et al. 2001; Conversely, periods of enhanced precipitation (i.e., Dore 2005; Wuebbles et al. 2014). pluvials) have been less examined despite similar (or even worse) negative socioeconomic impacts of these events such as mismanagement of water resources 2. Data and methods (Cook et al. 2011; Pederson et al. 2013), increased risk of a. Datasets floods or increased flood intensity (Pal and Eltahir 2002; Illston et al. 2004), and increased risk of wildfire in later Long-term datasets are required for our compre- years through buildup of biomass during the pluvial year hensive analysis of GP precipitation and relevant at- (Westerling et al. 2003, 2006). Yet, to gain a full un- mospheric variables. Precipitation data are from the derstanding of precipitation variability across the GP, Parameter-Elevation Regressions on Independent Slopes both pluvial and drought periods must be examined and Model (PRISM; Daly et al. 2000), which provides quantified. Most investigations into pluvial periods have monthly precipitation from 1895 to the present on a 4-km assumed that they are driven by conditions opposite to horizontal resolution. For atmospheric variables, we first that of drought and are thus focused on the influence of consider two monthly reanalysis products: the National global SSTs on synoptic flow patterns similar to drought Oceanic and Atmospheric Administration/Coopera- events (Yang et al. 2007; Schubert et al. 2008; Hu and tive Institute for Research in Environmental Sciences Huang 2009; Cook et al. 2011). Hu and Huang (2009) (NOAA/CIRES) Twentieth Century Reanalysis (20CR; found that GP precipitation anomalies are modified Compo et al. 2011) and the European Center for Medium- when phase alignment occurred between the Pacific Range Weather Forecasts (ECMWF) twentieth-century decadal oscillation (PDO) and El Niño–Southern Os- reanalysis (ERA-20C; Poli et al. 2016). Among these two cillation (ENSO), with enhanced forcing for wet pe- reanalysis products, the ERA-20C dataset better re- riods if PDO and ENSO were both in their warm produces the observed annual climatology of pre- phases and vice versa for their cold phases. Con- cipitation over the GP as depicted by PRISM (Fig. 1). versely, Cook et al. (2011) determined that tropical In addition, ERA-20C produces a larger dataset of Pacific SST anomalies had little explanatory power pluvial years for each composite compared to 20CR, during the central and western United States 1905–17 especially when the northern Great Plains (NGP; i.e., pluvial period and instead attributed the pluvial period North Dakota, South Dakota, and Nebraska) and to internal atmospheric variability. Moreover, Mo et al. southern Great Plains (SGP; i.e., Kansas, Oklahoma, (1997) illustrated the nonlinearity in the associated and Texas) subregions are considered, which provides a precursor patterns associated with pluvial and drought more robust subset of the data to calculate the com- events over the GP during the summertime. They found posite atmospheric fields. Thus, the 28328 ERA-20C that differences in eddy activity and subsequent mois- reanalysis dataset is selected to produce composites of ture transport over the GP were key to the pluvial atmospheric variables for this study and provides global event. Trenberth and Guillemot (1996) found that coverage of all
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