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Christopher M. Godfrey and David J. Stensrud

Planton 1989 ), which characterize the state of the land surface and forecast the evolution of the lowest layer of the model atmosphere. The surface energy balance relies strongly upon the soil and near-surface conditions and plays a critical role in determining the prognostic variables in land surface models. Vegetation coverage, atmospheric conditions, and the physical properties of the soil impact surface energy fluxes, which both influence and depend heavily upon soil temperature and soil moisture

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Jonathan E. Pleim and Robert Gilliam

1. Introduction The land surface components of meteorology modeling systems are responsible for the realistic representation of surface heat and moisture exchange processes and their dependence on vegetation and soil temperature and moisture. The surface fluxes of heat and moisture drive the near-surface air temperature and humidity and the evolution of the planetary boundary layer (PBL). The diurnal evolution of the PBL is of particular importance to air quality modeling applications. Thus

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Daniel Houle, Ariane Bouffard, Louis Duchesne, Travis Logan, and Richard Harvey

2080–99 for eastern North America ( Solomon et al. 2007 ). For the southern Quebec region, an ensemble of simulations project a warming between 3° and 5°C for 2080–99 and an increase in precipitation, mostly during winter and spring, between 5% and 17% ( Logan et al. 2011 ; DesJarlais et al. 2010 ). Projected changes are likely to affect soil moisture and temperature conditions, variables that have important impacts on many important processes such as seed germination and fine root development of

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Alexis Berg, Benjamin R. Lintner, Kirsten L. Findell, Sergey Malyshev, Paul C. Loikith, and Pierre Gentine

investigating the impact of land–atmosphere interactions on the distribution of daily surface temperature at the global scale with a focus on the role of soil moisture–atmosphere feedbacks. Soil moisture is a key variable in land–atmosphere interactions: the variations of soil moisture in response to atmospheric conditions (precipitation, radiation, and evaporative demand) impact surface turbulent and radiative heat fluxes, thereby potentially feeding back on atmospheric conditions. For example, low

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Jesse E. Bell, Michael A. Palecki, C. Bruce Baker, William G. Collins, Jay H. Lawrimore, Ronald D. Leeper, Mark E. Hall, John Kochendorfer, Tilden P. Meyers, Tim Wilson, and Howard J. Diamond

, for a workshop on the system design for a USCRN soil-climate–monitoring network (at the time of writing, a report from the workshop could be found online at the NIDIS U.S. Drought Portal at http://www.drought.gov/workshops/crn/USCRN_SMST_workshop_summary.pdf ). These discussions provided important input for the final decisions made by the USCRN program. The workshop members suggested the use of an instrument capable of measuring both soil moisture and temperature simultaneously, based on existing

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Zachary M. Subin, Charles D. Koven, William J. Riley, Margaret S. Torn, David M. Lawrence, and Sean C. Swenson

air temperature (SAT; precise definitions of common terms in appendix A , section a ) changes as the primary driver of soil temperature increases. However, other factors can be at least as important in determining soil temperature and active layer thickness (ALT; appendix A , section a ): the seasonally asymmetric presence of snow insulation (the snow thermal rectifier) is a major control on soil temperature ( Goodrich 1982 ; Zhang 2005 ). Many studies have shown the potential for changes in

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G. Balsamo, J-F. Mahfouf, S. Bélair, and G. Deblonde

and spatial resolution, and it appears a necessary development for global mesoscale NWP ( Viterbo and Courtier 1995 ; Koster et al. 2004 ; Ferranti and Viterbo 2006 ). In this paper, the development of a Canadian Land Data Assimilation System (CaLDAS) prototype for the land surface analysis in the NWP context at the Meteorological Service of Canada (MSC) is presented. The focus is put on soil moisture and temperature as principal components driving the water (e.g., through evapotranspiration

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R. J. Ronda and F. C. Bosveld

configuration, Heusinkveld et al. (2004) were able to measure the soil heat flux in the Negev Desert. In general, values of the thermal properties of the soil differ from thermal properties of heat flux plates that are used at measurement sites. In those situations, G 0 is inferred from a combination of heat flux plates that are placed at depths that are deeper than a few centimeters and one or more soil temperature sensors. The estimation of G 0 involves an extrapolation toward the surface, for which

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Laurel L. De Haan and Masao Kanamitsu

1. Introduction It has been well understood for many years that the response of general circulation models to tropical sea surface temperatures (SSTs) is of primary importance to climate prediction. However, it has become apparent more recently that soil moisture has an important secondary role. As a result, there has been an increased interest in understanding the impact of soil moisture on near-surface temperature and precipitation in general circulation models (GCMs). The influence of soil

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Clemens Schwingshackl, Martin Hirschi, and Sonia I. Seneviratne

role of soil moisture, since it affects various exchange processes at the surface. Seneviratne et al. (2010) provide an overview on the role of soil moisture for climate variability and land–atmosphere exchange. Based on both observational and modeling studies, various authors have shown that soil moisture has an impact on the evolution of near-surface air temperature ( Seneviratne et al. 2006 ; Koster et al. 2009b ; Jaeger and Seneviratne 2011 ; Seneviratne et al. 2013 ; Hirschi et al. 2014

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