Soil heat flux and day time surface energy balance closure at astronomical observatory, Thiruvananthapuram, south Kerala

Roxy, M.S.; Sumithranand, V B; Renuka, G.

doi:10.1007/s12040-014-0437-9

Cited by 18 publications

(10 citation statements)

References 29 publications

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“…Though the estimation of CCM was worse than the plate calorimetric method, CCM was better than FR on rain-free days, which was in good agreement with what Tyagi and Satyanarayana (2010) reported, i.e., the variation of G 0 from CCM was more reasonable than that from FR. Gao (2005) found that G 0 of CCM was more reliable than G 0 of the harmonic model by improving energy budget closure from 0.7 to 0.9 in Tibetan shortgrass prairie, while Roxy et al (2014) confirmed it as well.…”

Section: Conduction and Convection Modelmentioning

confidence: 89%

“…Accurate determination of ground soil heat flux, G 0 , is required to evaluate surface energy balance (de Silans et al 1997;Heusinkveld et al 2004;Roxy et al 2014), to estimate soil evaporation (Kampf et al 2005;Heitman et al 2010;Yao et al 2013), and to describe water and vapor transformation processes in vadose zone (Yamanaka et al 1997;Saito et al 2006;Bittelli et al 2008;Wang et al 2011aWang et al , 2011bZhang et al 2015). However, measurement of G 0 has still been a challenging task for researchers till now.…”

Section: Introductionmentioning

confidence: 99%

“…Horton and Wierenga (1983) developed the harmonic model to estimate G z using soil temperatures at two depths where soil temperatures can be described as Fourier series. Gao (2005) proposed conductionconvection model to estimate G z based on thermal conduction and convection processes in the soil profile, which produced a well estimation of G 0 (Roxy et al 2014).…”

Section: Introductionmentioning

confidence: 99%

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Estimation of ground heat flux from soil temperature over a bare soil

Wang

et al. 2016

Theor Appl Climatol

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Ground soil heat flux, G 0 , is a difficult-to-measure but important component of the surface energy budget. Over the past years, many methods were proposed to estimate G 0 ; however, the application of these methods was seldom validated and assessed under different weather conditions. In this study, three popular models (force-restore, conduction-convection, and harmonic) and one widely used method (plate calorimetric), which had well performance in publications, were investigated using field data to estimate daily G 0 on clear, cloudy, and rainy days, while the gradient calorimetric method was regarded as the reference for assessing the accuracy. The results showed that harmonic model was well reproducing the G 0 curve for clear days, but it yielded large errors on cloudy and rainy days. The force-restore model worked well only under rainfall condition, but it was poor to estimate G 0 under rain-free conditions. On the contrary, the conduction-convection model was acceptable to determine G 0 under rain-free conditions, but it generated large errors on rainfall days. More importantly, the plate calorimetric method was the best to estimate G 0 under different weather conditions compared with the three models, but the performance of this method is affected by the placement depth of the heat flux plate. As a result, the heat flux plate was recommended to be buried as close as possible to the surface under clear condition. But under cloudy and rainy conditions, the plate placed at depth of around 0.075 m yielded G 0 well. Overall, the findings of this paper provide guidelines to acquire more accurate estimation of G 0 under different weather conditions, which could improve the surface energy balance in field.

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Section: Conduction and Convection Modelmentioning

confidence: 89%

Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Estimation of ground heat flux from soil temperature over a bare soil

Wang

et al. 2016

Theor Appl Climatol

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“…Sauer and Horton (2005) summarized the advantages and disadvantages of the calorimetric, gradient, and combination methods, but point out that the gradient method is sensitive to λ, which can be difficult to estimate accurately for field conditions. Furthermore, these methods do not account for convection of heat by water movement (Evett et al, 2012a;Roxy et al, 2014). Evett et al (2012a) show that λ can be estimated for field conditions using a nonlinear fitting procedure of soil temperature measurements at successive depths and times.…”

Section: Calorimetric Methods For Gmentioning

confidence: 99%

Soil heat flux calculation for sunlit and shaded surfaces under row crops: 1. Model development and sensitivity analysis

Colaizzi

Evett

Agam

et al. 2016

Agricultural and Forest Meteorology

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Mention of company or trade names is for description only and does not imply endorsement by the USDA. The USDA is an equal opportunity provider and employer. Abbreviations: a = empirical constant used in surface soil heat flux model (no units); BEG = beginning period of the study during sparse canopy cover; C zj = volumetric heat capacity of the soil in layer j (J m-3 K-1); END = end period of the study during full or nearly full canopy cover; EW = east-west crop row orientation; f o,zj = volume fraction of organic matter at depth z j (m 3 m-3); f SIS = fraction of shading of an interrow section (no units); G 0 = soil heat flux at the soil surface (W m-2); G 0,MAX = maximum G 0 over 24 h (midnight to midnight) (W m-2); G 0,MIN = minimum G 0 over 24 h (midnight to midnight) (W m-2); G Z = soil heat flux measured at z p (W m-2); MID = middle period of the study during intermediate canopy cover; NS = north-south crop row orientation; R N = total net radiation (W m-2); R N,S = soil net radiation (W m-2); R N,S,MAX = maximum R N,S over 24 h (midnight to midnight) (W m-2); R N,S,MIN = minimum R N,S over 24 h (midnight to midnight) (W m-2); S M = model sensitivity (no units); t i and t i+1 = time at successive time steps i and time i+1 (s); T S,0 = soil surface temperature (K); T s,z = soil temperature at depth z (K); z j = depth of the midpoint of soil layer j (m); z p = depth below the soil surface of soil heat flux plates (m); ΔG 0,Zp = divergent heat flux into the soil layer between z p and soil surface (W m-2); Δz j = thickness of soil layer j (m); θ v,zj = volumetric soil water content at depth z j (m 3 m-3); λ = soil thermal conductivity (J s-1 m-1 K-1); ρ b,zj = soil bulk density at depth z j (Mg m-3).

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“…Available net radiation is the balance between incoming and outgoing radiation which is the main source of energy in the earth system. The balance of energy at the earth's surface is closely associated with the overlying atmospheric boundary layer (Roxy et al, 2014). The total available energy and partitioning of it into different components such as sensible heat (h), latent heat (LE) and soil heat fluxes (G) influences the production of the crop very strongly.…”

Section: Introductionmentioning

confidence: 99%