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Eleanor J. Burke

, drought occurring 100% of the time. Soil moisture and precipitation drought occur less frequently than PDSI drought, with a tendency for soil moisture drought to be more frequent than precipitation drought. Fig . 2. The subset of Giorgi and Francisco (2000) regions used within the analysis: CNA = central North America; CAM = Central America; AMZ = Amazon; WAF = western Africa; SAF = South Africa; MED = Mediterranean; SAS = southern Asia; SEA = Southeast Asia; NAU = northern Australia; SAU = southern

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Nurit Agam (Ninari) and P. R. Berliner

direct absorption). Moreover, the gains in soil water content during the night are compared to the dew amounts recorded by the Hiltner balance, and the losses and gains of water in terms of easily measurable environmental parameters are parameterized. 2. Materials and methods The measurements were carried out at the Wadi Mashash Experimental Farm in the northern Negev, Israel (31°08′N, 34°53′E; 400 m MSL, 60 km from the Mediterranean Sea). Rainfall events occur between October and April, and the mean

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Bert G. Heusinkveld, Simon M. Berkowicz, Adrie F. G. Jacobs, Albert A. M. Holtslag, and Willy C. A. M. Hillen

the base. 3. Field site description Two load cell microlysimeters were tested during a 6-week field campaign held in September–October 2000, in the Hebrew University of Jerusalem Minerva Arid Ecosystems Research Center (AERC) sand dune experimental station (30°56′N, 34°23′E; elevation 190 m msl) situated near Nizzana, northwest Negev Desert, Israel. The Mediterranean Sea lies about 40 km to the northwest. The average annual rainfall of the region is about 100 mm, with a coefficient of variation of

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Huade Guan, Xinping Zhang, Oleg Makhnin, and Zhian Sun

coastal proximity) is due to different thermal properties between land and water bodies and the processes induced by this contrast, including sea breezes and land breezes. Longitude (or easting) is also commonly used in the multiple-regression models. Its physical connection to temperature distribution is less clear. Depending on locations, it may reflect the effect of the distance to a source of warm or cold air mass (e.g., ocean, continent, ridge, or city). Similarly, latitude (or northing) can be

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Daniel G. Kingston, Anne K. Fleig, Lena M. Tallaksen, and David M. Hannah

. , 2011 : Predictability of Mediterranean climate variables from oceanic variability. Part 1: Sea surface temperature regimes . Climate Dyn. , 36 , 811 – 823 . Hu, Z. , and Huang B. , 2006 : Air–sea coupling in the North Atlantic during summer . Climate Dyn. , 26 , 441 – 457 . Hurrell, J. W. , and van Loon H. , 1997 : Decadal variations in climate associated with the North Atlantic Oscillation . Climatic Change , 36 , 301 – 326 . James, P. M. , 2007 : An objective classification

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M. Petracca, L. P. D’Adderio, F. Porcù, G. Vulpiani, S. Sebastianelli, and S. Puca

to define potentialities and limitations in the use of GPM-DPR products as reference for the validation of the H SAF precipitation products over the MSG full disk. Italy is an ideal test bed for complex terrain in a Mediterranean climatic regime, as it consists of a mixture of mountainous terrain (Alps, Apennines) and flatter/coastal areas. The country is well instrumented by a network of 22 weather radars ( Vulpiani et al. 2014 ; Rinollo et al. 2013 ), as well as a network of around 3000 rain

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Xing Yuan, Eric F. Wood, Nathaniel W. Chaney, Justin Sheffield, Jonghun Kam, Miaoling Liang, and Kaiyu Guan

( Camberlin et al. 2001 ). Recently, the Indian Ocean and Mediterranean Sea are receiving more attentions for their contributions to the rainfall variability over eastern and northern Africa, respectively ( Bowden and Semazzi 2007 ; Gimeno et al. 2012 ). These teleconnections have been used to form the basis for developing statistical approaches in forecasting drought at seasonal scales ( Barnston et al. 1996 ; Mason 1998 ). On the other hand, atmosphere–ocean–land coupled general circulation models

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Wenguang Wei, Zhongwei Yan, and P. D. Jones

usually a driving process behind it (e.g., global warming and transition from one to another phase of some large-scale climate oscillation). For Xinjiang in northwestern China, previous studies have shown that, during the past half century, increasing atmospheric water vapor mainly comes from the North Atlantic and the Arctic Ocean for summer and from the Caspian Sea and the Mediterranean for winter ( Dai et al. 2007 ). A major increase of the water vapor in Xinjiang happened in the middle of the 1980

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Daniel G. Kingston, Glenn R. McGregor, David M. Hannah, and Damian M. Lawler

climate indices: The North Atlantic Oscillation, El Nino Southern Oscillation and beyond. Proc. Roy. Soc. London , 270B , 2087 – 2096 . Stewart, I. T. , Cayan D. R. , and Dettinger M. D. , 2005 : Changes toward earlier streamflow timing across western North America. J. Climate , 18 , 1136 – 1155 . 10.1175/JCLI3321.1 Struglia, M. V. , Mariotti A. , and Filograsso A. , 2004 : River discharge into the Mediterranean Sea: Climatology and aspects of the observed variability. J

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A. Verhoef, A. Diaz-Espejo, J. R. Knight, L. Villagarcía, and J. E. Fernández

vapor pressure gradient and hence favors adsorption. This increase in h a , or at least the leveling off of its sharp decline started during the morning, is caused by a sudden change in wind direction, from southeast to southwest, bringing in moister air that originates from the Mediterranean Sea (approximately 80 km to the southwest of the Coria experimental site). Vapor adsorption is larger for the OLS than for the ILS. Significant vapor adsorption generally ceases around 1800 UTC, because e s

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