EffectsofSummerRainfallontheSoilThermalPropertiesand SurfaceEnergyBalancesintheBadainJaran… · e Badain Jaran Desert is host to a variety of wavy landformsandsandmountains,thelatterofwhicharethe

Research ArticleEffects of Summer Rainfall on the Soil Thermal Properties andSurface Energy Balances in the Badain Jaran Desert

Jiangang Li 12 AliMamtimin 12 Zhaoguo Li3 Cailian Jiang4 andMinzhongWang 12

1Institute of Desert and Meteorology CMA Urumqi 830002 China2Center of Central Asian Atmospheric Science Research Urumqi 830002 China3Key Laboratory of Land Surface Process and Climate Change in Cold and Arid RegionsNorthwest Institute of Eco-Environment and Resources Chinese Academy of Sciences Lanzhou 730000 China4Wujiaqu Meteorology Bureau Wujiaqu 831300 China

Correspondence should be addressed to Ali Mamtimin aliidmcn

Received 20 April 2019 Revised 11 October 2019 Accepted 13 November 2019 Published 6 December 2019

Academic Editor Stefano Dietrich

Copyright copy 2019 Jiangang Li et al is is an open access article distributed under the Creative Commons Attribution Licensewhich permits unrestricted use distribution and reproduction in any medium provided the original work is properly cited

Based on observational data collected during the summer of 2009 from the southern Badain Jaran Desert the surface sensible andlatent heat fluxes and shallow soil thermal storage were obtained through corrections and quality control measures e soil thermalproperties and characteristics of the land surface energy budget before and after rainfall episodes were systematically analyzed Short-term precipitation had a greater influence than systematic precipitation on the soil temperature (ST) and soil volumetric watercontent (VWC) After rainfall the VWC rapidly increased showing a decreasing growth rate trend with depth and time in all layersthe soil temperature change rate (TCR) exhibited the opposite tendency e surface albedo which was affected little by the solarelevation angle and short-term precipitation fluctuated from low to high during short-term rainfall e soil thermal parametersincluding the volumetric heat capacity thermal conductivity and diffusivity all increased after rainfall e diurnal soil heat fluxvariations in each layer manifested as quasisinusoids and the amplitude gradually decreased with depth e energy balance ratio(EBR) without and with soil heat storage (S) varied differently after incorporating S the EBR increased by approximately 5-6regardless of rainfall but remained lower afterward roughout the observation period the maximum daytime EBR appearedapproximately 1-2 days before or after rainfall and gradually declined otherwise ese findings are fundamental for understandingthe influences of cloud and precipitation disturbances on radiation budgets and energy distributions and improving the param-eterization of surface radiation budgets and energy balances for numerical models of semiarid areas

1 Introduction

Global warming not only leads to an increase in air tem-perature but also changes the amount intensity and fre-quency of precipitation [1] Since the 20th century theprecipitation falling over the mid-high latitudes of theNorthern Hemisphere has increased by approximately 7ndash12 but the spatial distribution of this precipitation isuneven and exhibits a high degree of heterogeneity whichresults in both an increased degree of uncertainty regardingthe occurrence and duration of extreme precipitation and anenlargement of drought areas e latter phenomenon in-tensifies hydrologic processes in terrestrial ecosystemsparticularly in arid and semiarid areas [2 3]

While partitioning of land surface fluxes the soil has alarger role to play on the hydrological cycle as they are tightlyconnected with both land-atmosphere energy and waterexchanges [4 5] Previous studies have shown that soil has aprofound impact on the atmospheric surface layer and thedistribution and characteristic parameters of soil havecertain effects on land-atmosphere energy exchange waterexchange and the hydrological cycle [6ndash8] e transport ofboth soil heat and water from the land surface to deeperlayers is closely related to soil structure parameters such asthe soil composition volume-weight ratio humidity andsoil thermal parameters including the soil thermal con-ductivity thermal capacity thermal diffusivity and specificheat [9] Accordingly some researchers have studied the

HindawiAdvances in MeteorologyVolume 2019 Article ID 4960624 13 pageshttpsdoiorg10115520194960624

thermal properties and heat fluxes of soil using a variety ofmethods and products [10ndash15] including the NOAH LandSurface Model (LSM) for estimating net radiation and latentsensible and ground heat (GH) fluxes as well as waterbalance components in four land treatments [16] a hy-drological model for the simulation of soil moisture acrossmultiple depths [17]

e majority of arid regions in Northwest China aredesert or Gobi and are subject to intense solar radiation as aresult the soil parameters are vastly different from those oftypical regions and the land surface physical processestherein exhibit notable regional characteristics [18] Sincethe late 1980s comprehensive field experiments have beencarried out on land surface processes e Heihe River fieldexperiment (HEIFE) and the field experiment on the air-land interaction in the arid area of Northwest China (NWC-ALIEX) have confirmed certain soil parameters in the soilsurface of their research regions [19ndash22] However com-paratively speaking specific research on the soil parametersin arid regions is still limited

As the main water source in desert areas precipitationhas a considerable impact on themovement of dunes and thedistribution of vegetation [23ndash27] Due to limitations posedby the natural environment only a small number of ob-servation stations with an uneven spatial distribution aresituated in the arid desert area of Northwest China as aresult the characteristics of the soil physical parameterstherein specifically in the untraversed desert hinterlands arepoorly understood Nevertheless local meteorologists haveconducted a large amount of research in the Taklamakan andGurbantunggut Deserts and their work has resulted innumerous achievements with regard to the effects of pre-cipitation on deserts and their surrounding areas [28ndash30]

e Badain Jaran Desert is host to a variety of wavylandforms and sand mountains the latter of which are thehighest in the world and these landforms have profoundeffects on rainfall Zhang et al analyzed the rainfall distri-bution in this region based on data from meteorologicalstations located around the desert [31] However few studieshave investigated the effects of rainfall on the thermalproperties of soil in deserts

In this paper hourly rainfall data acquired during theintense observation period (IOP hereinafter) in the BadainJaran Desert hinterland were integrated Basic data in-cluding the surface sensible heat flux latent heat flux andshallow soil thermal storage data were obtained and thesurface albedo soil volumetric heat capacity thermal con-ductivity thermal diffusivity and energy balance ratio (EBR)were calculated by relevant equationse effects of differenttypes of rainfall on these soil characteristics and on thesurface energy balances were analyzed the results of whichreveal the energy and water distributions in the underlyingsurface layer throughout the arid region of Northwest China

2 Materials and Methods

21 Materials e Badain Jaran Desert located in the AlxaBanner of Inner Mongolia at approximately 395degndash42degN and985degndash104degE is the second-largest desert in China with an

area of approximately 52000 square kilometers [32] isdesert is mainly influenced by westerlies namely the Indianand East Asian monsoons and belongs to temperate aridand extremely arid climate zones e average annualprecipitation exhibits a decreasing trend from the southeast(approximately 120mm) to the northwest (less than 40mm)[33] precipitation primarily occurs from July to Augustenorthwest arid area which is subject to a large amount ofevaporation and abundant sunshine is sensitive to climatechange and possesses a fragile ecological environmentHence the northwest arid area is considered an ideal site toobserve the water and heat exchanges in the underlyingdesert surface

From June to September of 2009 researchers carried outa series of field observation experiments in the hinterland ofthe Badain Jaran Deserte observation points were locatedin the southeast of the desert (39deg28122primeN and 102deg22365primeEat an altitude of 1418m)e D1 observation site which wassurrounded by an open undulating yellow sand terrain is acharacteristic desert area Sparse vegetation was distributedapproximately 500sim700m from the observational stationmost of which was Alhagi sparsifolia and Nitraria tangu-torum Bobr was also present (as shown in Figure 1)

e air temperature and humidity wind precipitationsoil temperature (ST hereinafter) and soil moisture (volu-metric water content VWC hereinafter) land surface ra-diation and turbulence were observed e IOP lasted fromJune 21st to September 12th In this paper the local standardtime (LST hereinafter) which was 7 h ahead of CoordinatedUniversal Time (UTC) was selected for the calculation andanalysis

e data from August 4th to September 20th were se-lected for analysis to reflect the effects of rainfall on the soilthermal properties and energy balances in the desert hin-terland During this period there were two large-scaleprecipitation events one occurred on August 18th with29mm of precipitation and the other occurred on September5ndash7th with 226mm of total precipitation ese eventsrepresent rare phenomena in this extremely arid desert area

22 Methods e hourly precipitation distributions of thetwo aforementioned synoptic processes are shown in Fig-ure 2 which shows that the first weather event (August 18th)had a short precipitation duration with a high intensity themaximum rainfall intensity reached 78mmmiddothminus 1 In contrastthe second weather event had a longer duration but themaximum intensity was only 28mmmiddothminus 1 is result in-dicates that the two precipitation processes were notablydifferent the first weather event was an extremely intenserainfall episode the sort of which is typical in the arid regionof Northwest China while the second weather event wascharacteristic of systematic rainfall

e sampling frequency of the surface turbulence datawas 10Hz while the radiometer and soil heat flux plategenerated average ST and VWC values respectively every30min Basic data quality control measures such as outlierelimination time delay correction virtual temperature cor-rection and WebbndashPearmanndashLeuning (WPL) correction

2 Advances in Meteorology

were applied To enhance the comparability only data thathad been averaged over 05 h intervals and controlled forquality were used for analysis in this paper

e surface sensible heat flux (H) and latent heat flux(LE) were calculated by the eddy covariance method [34]

H ρlowastCP lowastwprimeθprime (1)

LE ρlowast λlowastwprimeqprime (2)

In formulas (1) and (2) ρ is the air density CP is thespecific heat at a constant pressure and λ is the latent heat ofevaporation the latter two are constants wprimeθprime and wprimeqprime are

statistics of the turbulent quantities of the wind temperatureand humidity respectively

e water-bearing soil volumetric heat capacity Cswater-free soil volumetric heat capacity Csd thermal con-ductivity λsi and thermal diffusivity Ksi were calculatedaccording to the following formulas [35]

cs G1 minus G2

Δzlowast zTgzt1113872 1113873 (3)

csd G1 minus G2( 1113857 minus Vw lowastCw lowastΔzlowast zTgzt1113872 1113873

Δzlowast zTgzt1113872 1113873 (4)

Gansu

Qinghai

InnerMongolia

NingxiaEjina Qi

Guaizi lake

Bayinnuorigong

Alxa Right Banner

D1

Zhangye

Gaotai

Dingxin

Jinta

0 35 70 140 210Km

N

99degE 100degE 101degE 102degE

39degN

40degN

41degN

42degN

103degE 104degE 105degE

Weather stationObservation stationDesert region

Figure 1 Observation site and surface conditions in the Badain Jaran Desert

90

80

70

60

50

40

30

20

10

00

(Aug 18)TimeLST

Prec

ipita

tion

(mm

)

0000 0200 0400 0600 0800 1000

(a)

30

20

10

000000 0800 1600 0000 0800 1600 0000

(Sep 5) (Sep 6) (Sep 7)TimeLST

Prec

ipita

tion

(mm

)

(b)

Figure 2 Hourly precipitation distributions of the two weather events (a) August 18th (b) September 5ndash7th

Advances in Meteorology 3

λsi Gi

zTgzz (5)

Ksi λsiCs

(6)

In formula (3) G1 and G2 are the two observed soil heatflux values in the upper (5 cm) and lower (20 cm) layersrespectively Δz is the thickness between the two observationlayers and zTgzt represents the average ST change ratebetween the observation depths of the soil heat flux in thetwo layers In formula (4) Vw is the soil volumetric watercontent and Cw is the specific heat of water which is42lowast103 J(kgmiddotdegC) In formula (5) Gi is the heat flux of thedesired soil depth and zTgzz represents the vertical STgradient

Since it was difficult to directly measure the surface heatflux in this paper the thermal storage in the shallow soillayer was calculated with the thermal diffusion equation andcorrection (TDEC) method [36] at is the surface heatflux was derived by using the measured 5 cm soil layer heatflux and the soil thermal storage of the above 5 cm layer asfollows

Gsfc Gz + S (7)

S 1113946zzref

z0ρs lowastCs lowast

zT

ztdz (8)

In formula (7) Gz and S represent the soil heat flux andthermal storage of the 5 cm layer respectively In formula(8) ρs is the soil density which is 16lowast103 kgmiddotmminus 3 [37] Cs isthe soil specific heat zref is the reference depth which is005m and zTzt represents the temperature change ratebetween the surface and reference depth

e following calculation formulas were employed forthe surface net radiation Rn albedo α and EBR

Rn RSD + RLD minus RSU minus RLU (9)

α RSU

RSD (10)

EBR 1113936(H + LE)

1113936 Rn minus Gsfc minus S( 1113857 (11)

In formulas (9) and (10) RSD RLD RSU andRLU rep-resent the total solar radiation atmospheric longwave ra-diation surface reflective radiation and surface longwaveradiation respectively In formula (11) Gsfc is the surfaceheat flux and S is the canopy heat storage capacity which isequal to zero in the desert area

3 Results

31 Effects of Rainfall on ST and VWC Figure 3 shows thevariations in the ST and before and after rainfall during thetwo rainfall episodes Figure 3(a) shows that the VWC valuesat depths of 5ndash20 cm were almost equal and the increase inthe VWC value at 40 cm was larger before the first rainfall

episode than before the second episode With the infiltrationof rainwater the VWC increased rapidly and the VWCincrease from shallow to deep layers exhibiting a decliningtrend similar to the result of research in the NebraskaSandhills [27] Based on the change in the VWC in each layerwith time the VWC was delayed 15 h at depths of ap-proximately 5ndash20 cm and 4 h at depths of 20 and 40 cmAfter each rainfall episode the VWC tended to decrease andthe lapse rate at depths of approximately 5ndash20 cm was largerthan that at a depth of 40 cm and decreased with timeDuring the second rainfall episode as the rainfall intensitywas relatively small the growth rate of the VWC was lessnotable than that during the first rainfall episode e lagtime of the VWC change in each layer was notably pro-longed with a 6 h delay at depths between 20 and 40 cm

Figure 3(b) shows the variations in the soil temperaturechange rate (TCR hereafter) before and after the first rainfallepisode in various layers Evidently the TCR at a depth of5 cm before rainfall was in the range of minus 3 to 4degC with adistinct diurnal variation cycle while the variability in otherlayers decreased with increasing depth is phenomenonindicates that the soil was dry possessed a suitable heattransfer capacity and was easily influenced by solar radia-tion in the shallow layer After rainfall the TCR notablyincreased and was negative at depths of approximately 5ndash10 cm indicating that the short-term precipitation caused arapid decrease in the ST while having little effect on thedeeper soil layers During the second rainfall episode theTCR was similar to that during the first rainfall episode butits variation was clearly smaller with a longer durationHowever in the deeper layers the TCR increased to largervalues than those during the first rainfall episode thisdiscrepancy was related to the slow long-term infiltration ofrainwater

To compare the diurnal variation trends of the TCRbetween the soil and air the mean diurnal air TCR andcorresponding soil TCR were calculated on rainy and cleardays for the entire period as shown in Figure 4 As rainfallfell the air TCR changed quickly while the soil TCRgradually decreased and was lagged by approximately 1 hsuccessively at depths from 5 cm to 20 cm however the TCRat a depth of 40 cm changed very little and was lagged byapproximately 5 h behind that at a depth of 20 cm(Figure 4(a)) Figure 4(b) shows the same diurnal trends butthe variation in the air TCR was more obvious on clear daysAlthough there were rapid changes in the air TCR theoverall diurnal trend was consistent with its soil counterpartregardless of the weather

32 Effects ofRainfall on the SurfaceAlbedo Variations in thesoil color roughness length VWC and solar elevation anglecan change the surface albedo [38 39] As shown in Figure 1the short-term intense rainfall had a greater impact on theVWC than the long-term systematic rainfall so the firstrainfall episode was selected for analysis

Figure 5(a) shows that the change in the surface albedobefore and after precipitation was not significant but thesurface albedo exhibited a clear reduction during the rainfall


episode Figure 3(a) also demonstrates that the VWC at adepth of 5 cm decreased the fastest after rainfall while thesurface albedo recovered to a state that was similar to that onthe sunny day before the rainfall episode Additionally thevariation in the surface albedo on the 18th also indicates thatthe albedo first decreased and then increased due to theincrease in the VWC in the surface layer after rainfallleading to a decrease in the surface albedo With increasingsolar elevation angle and surface temperature evaporationincreased and the VWC started to decrease while thesurface albedo increased ese trends are similar to thoseobserved in the degraded grasslands of semiarid areas [40]

Figure 5(b) shows the variations in the surface albedowith the solar elevation angle in the desert area According tothe calculations when the solar elevation angle was greaterthan 25deg the effect on the surface albedo was very limitedwhich is somewhat different from the results obtained in theTaklimakan Desert [41] is difference was caused mainlyby the latitude difference between the two locations Cal-culations reveal that the solar elevation angle at 7 00 LST inthe middle of August was approximately 20-21deg in the studyarea erefore the solar elevation angle had little effect onthe surface albedo before and after rainfall instead thealbedo was related to the smooth underlying surface and lesspronounced topographic undulation in the desert

33 Effects of Rainfall on the Soil ermal ParametersFigure 3 shows that the ST and VWC varied greatly beforeand after the rainfall event on August 18thus periods of aweek before and after the rainfall episode (August 12ndash24th)were selected for analysis where August 12ndash17th and August19ndash24th were chosen as the periods before and after therainfall episode respectively

Figure 6(a) shows that the soil thermal capacity beforethe rainfall event was 109times106 Jmiddotmminus 3middotKminus 1 which is close tothe measured value of 112times106 Jmiddotmminus 3middotKminus 1 [42] in Dunhuangand slightly lower than the result of 156times106 Jmiddotmminus 3middotKminus 1 inthe Taklimakan Desert [41] After rainfall (Figure 6(b)) thesoil thermal capacity increased to 154times106 Jmiddotmminus 3middotKminus 1 due tothe increase in the VWC and a lower air content betweensand particles which resulted in an increase in the soilthermal capacity As shown in Figures 6(c) and 6(d) thewater-free soil thermal capacity increased notably before andafter rainfall respectively

To better understand the influence of the VWC on thesoil heat capacity the variations in the soil thermal capacitywith the VWC in the water-bearing and water-free soils afterrainfall were analyzed as shown in Figure 7e two kinds ofsoil exhibited similar trends the soil thermal capacity slowlyincreased with increasing soil VWC

Figure 8 shows that the soil thermal conductivity at adepth of 5 cm (in the shallow layer) before rainfall was only023Wmiddotmminus 1middotKminus 1 which is close to the measured value in thehinterland of the Taklimakan Desert after rainfall the valuemore than doubled to 066Wmiddotmminus 1middotKminus 1 e soil thermalconductivity at a depth of 20 cm after rainfall was approxi-mately 5 times that before rainfall From a vertical depthperspective the soil thermal conductivity in the middle layerwas only slightly higher than that in the shallow layer beforerainfall but was twice that in the shallow layer after rainfalle main reason for this phenomenon is that the solar ra-diation of the middle layer before rainfall was smaller due to ahigher VWC e aforementioned conditions resulted in asmall thermal conductivity difference between the middle andshallow layers due to the dry yellow sand surface covering thedesert (Figure 3(a)) After rainfall similar to the principlegoverning the increase in the soil thermal capacity the VWC

012

010

008

006

004

002

(a)

(b)4030201000

ndash10ndash20ndash30ndash40

Date

5cm10cm

20cm40cm

Aug 4 Aug 10 Aug 16 Aug 22 Aug 28 Sep 3 Sep 9 Sep 21Sep 15

Soil_

VW

C (m

3 middotmndash3

)So

il_TC

R (deg

Cmiddothndash1

)

Figure 3 Variations in ST and VWC before and after rainfall (a) VWC and (b) TCR


values in the middle and shallow layers exhibited a decliningtrend due to evaporation A soil moisture inversion phe-nomenon appeared before August 22nd but gradually dis-appeared afterwarde VWC at a depth of 20 cmwas greaterthan those at the other depths erefore there was a largevariation in the soil thermal conductivity in the middle layer

after rainfallis finding ultimately indicates that rainfall hada large effect on the soil above a depth of 20 cm while theeffect on the soil below 20 cm was relatively small

e soil thermal diffusivity represents the instantaneouschange in STwith the given boundary conditions Accordingto the formulas in this paper the soil thermal diffusivity

Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time

20cm40cm

Air5cm10cm

0000 0400 0800 1200 1600 2000 2400

(a)

20cm40cm

Air5cm10cm

Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time0000 0400 0800 1200 1600 2000 2400

(b)

Figure 4 Diurnal TCR variation in the air and in each layer (a) rainy days and (b) clear days

06

05

04

03

02

Alb

edo

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

(a)

06

05

04

03

0210 20 30 40 50 60 70

Alb

edo

Solar elevation angle (deg)

(b)

Figure 5 (a) Variations in the surface albedo before and after rainfall (the dashed-dotted rectangle represents the short-term rainfallperiod) (b) variations in the surface albedo at different solar elevation angles


values before and after rainfall were calculated as21times 10minus 7m2middotsminus 1 and 43times10minus 7m2middotsminus 1 respectively at adepth of 5 cm and 28times10minus 7m2middotsminus 1 and 94times10minus 7m2middotsminus 1respectively at a depth of 20 cm

Based on the above analysis the rainfall episodes hadconsiderable effects on the soil thermal parameters in thedesert area indicating that the soil volumetric heat capacitythermal conductivity and thermal diffusivity after rainfall all

R2 = 086y = 109x + 108

100

50

0

ndash50

∆zlowast(∆Tg∆t) (10ndash6mmiddotKmiddotsndash1)

∆G (W

middotmndash2

)

ndash50 0 50 100

(a)

120

60

0

ndash60ndash60 0 60 120

R2 = 093y = 154x + 024


∆G (W

middotmndash2

)

(b)

100

50

0

ndash50

R2 = 084y = 098x + 107

∆G (W

middotmndash2

)

∆zlowast(∆Tg∆t) (10ndash6mmiddotKmiddotsndash1)ndash50 0 50 100

(c)

R2 = 090y = 125x + 021

100

50

0

ndash50

∆G (W

middotmndash2

)


(d)

Figure 6 Variations in the soil thermal capacity before and after rainfall (a) water-bearing soil before rainfall (b) water-bearing soil afterrainfall (c) water-free soil before rainfall (d) water-free soil after rainfall

30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)

VWC (m3middotmndash3)0060 0065 0070 0075 0080 0085

(a)

30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(b)

Figure 7 Variations in the soil thermal capacity with the VWC (a) water-bearing soil and (b) water-free soil


significantly increased in comparison with those beforerainfall Moreover the growth rates of the soil thermalconductivity and thermal diffusivity in the middle layer werenotably higher than those in the shallow layer Moreoverwith respect to the Dunhuang Gobi and hinterland of theTaklimakan Desert the soil thermal conductivity andthermal diffusivity in the Badain Jaran Desert were slightlyhigher

34 Effects of Rainfall on the Surface Energy Balance e soilheat flux is an integral part of the surface energy balance andplays an important role in the distribution of surface energyCorrectly estimating the soil heat flux can significantlyimprove the surface energy imbalance particularly in bare orsparsely vegetated ground [43]

Figure 9(a) shows the variation in the global solar ra-diation before and after the first rainfall episodeeweatherwas clear with dry air and a suitable atmospheric trans-parency before rainfall accordingly the diurnal variationcurve of the global solar radiation was relatively smooth andthe daily extremes were all close to 1000Wmiddotmminus 2 e latterobservation indicates that the solar radiation in the desert

was intense at this time Additionally because rainfallusually occurred in the nighttime its effect on solar radiationwas less pronounced After the rainfall event the weathergradually cleared up but clouds easily formed due to thelarge amount of water vapor evaporation and atmosphericvertical motion resulting in reduced solar radiationerefore the daily global solar radiation peak decreasedslightly after rainfall with respect to that before rainfall

Figure 9(b) shows the variations in the soil heat flux atdepths of 5 and 20 cm before and after rainfall Clearly thesoil heat flux exhibited distinct diurnal variations resemblingquasisinusoids in all layers Moreover these fluctuationsgradually decreased with increasing depth With respect tothat in the shallow layer the variation in the soil heat flux inthe middle layer before and after rainfall lagged by ap-proximately 4 h Furthermore the solar radiation wasweaker during the rainfall episode than before or afterCompared with the atmosphere the land surface became acold source Soil heat was released from deeper layers to thesurface layer and thus the surface layer exhibited a largenegative value (shown in the dotted box in Figure 9(b))Even under the circumstances involving a small variation inthe total radiation the fluctuation in the soil heat flux in all

R2 = 085y = 023x + 1352

100

70

40

10

ndash20

ndash50

(∆Tg∆z) (degCmiddotmndash1)

G5 (

Wmiddotm

ndash2)

ndash200 ndash150 ndash100 ndash50 0 50 100 150 200

(a)

200

150

100

50

0

ndash50

ndash100

ndash150ndash150 ndash100 ndash50 0 50 100 150 200

R2 = 086y = 066x + 264


G5 (

Wmiddotm

ndash2)

(b)

R2 = 068y = 031x + 050

20

10

0

ndash10ndash20 ndash10 0 10 20 30 40


G20

(Wmiddotm

ndash2)

(c)

50

30

10

ndash10

ndash30

R2 = 095y = 145x ndash 010

ndash20 ndash10 0 10 20 30(∆Tg∆z) (degCmiddotmndash1)

G20

(Wmiddotm

ndash2)

(d)

Figure 8 Variations in the soil thermal conductivity before and after rainfall (a) 5 cm depth before rainfall (b) 5 cm depth after rainfall (c)20 cm depth before rainfall (d) 20 cm depth after rainfall


layers after rainfall increased in comparison with that beforerainfall e cause of this enhanced fluctuation is attributedto the decrease in the surface albedo after rainfall the relativeincrease in the amount of heat entering the soil and thesignificant increases in the soil thermal parameters in-cluding the soil volumetric heat capacity compared withthose before rainfall As a result the soil absorbed a largeramount of heat in the daytime and released a larger amountof heat in the nighttime

Figures 10(a) and 10(c) depict the variations in theEBR without S (thermal storage in the 5 cm layer) beforeand after rainfall respectively during the daytime (08 00ndash17 00 LST) ese figures demonstrate that the EBRwhich was 062 before rainfall decreased to 050 after therainfall episode Two reasons can explain this phenom-enon On the one hand in this desert area the vegetationwas sparse the latent heat on a sunny day was small andthe surface energy was transported primarily by sensibleheat [44] erefore the surface sensible heat flux reacheda maximum value of 400Wmiddotmminus 2 whereas the daily latentheat flux extreme reached only approximately 45Wmiddotmminus 2Although the VWC increased after rainfall resulting in anotable increase in the latent heat flux with a maximumexceeding 150Wmiddotmminus 2 the latent heat flux decreasedrapidly with the gradual decline in the VWC Howeverthe sensible heat flux decreased after rainfall due tovariations in the soil thermal properties and weathereffects As a result the turbulent energy (calculated asHs + LE) was notably reduced On the other hand al-though the soil heat flux at a depth of 5 cm after rainfall

slightly increased (Figure 9(b)) the net radiation slightlydecreased due to the reduction in the global solar radi-ation As a result the effective energy (calculated asRnminus G) slightly decreased

e EBR values with S before and after rainfall are shownin Figures 10(b) and 10(d) respectively Clearly the EBRwith S increased approximately 5-6 before and afterrainfall indicating that S in the surface layer had an im-portant contribution to the surface energy balance in thisdesert area From these figures the EBR with S after rainfallwas still lower than that before rainfall e main reason forthis phenomenon is that the soil thermal capacity anddensity both increased with increasing VWC in the shallowlayer after rainfall As a result S became larger intensifyingthe surface energy imbalance

Figure 11 shows the overall variation trends in the EBRin the daytime before and after the two rainfall episodesClearly the EBR increased slowly because of the suitableweather conditions before rainfall and reached a maximumvalue that was affected by the surface properties and weatherconditions After rainfall the EBR gradually decreased againAdditionally the EBR after rainfall was slightly lower thanthat before rainfall Figure 10(b) shows that the average EBRwith S was 061 which represented an increase of 6 incomparison with that without S

e above analysis illustrates that the EBR remained lowduring both the short-term and the systematic rainfall ep-isodes as a result of the profound energy imbalance in thedesert area Many reasons were responsible for this phe-nomenon which requires further study

Global radiation

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

5cm20cm

Glo

bal r

adia

tion

(Wmiddotm

ndash2)

Soil

heat

flux

(Wmiddotm

ndash2)

1200 (a)

(b)

1000

800

600

400

200

0

150

100

50

0

ndash50

ndash100

Figure 9 Variations in the (a) global solar radiation and (b) soil heat flux before and after rainfall


4 Discussion

e annual precipitation and number of annual rainy days atthe tops of the sand mountains in the Badain Jaran Desertwere slightly higher than those in the fields surrounding thehills [45] thus the responses of the soil properties to rainfallin different desert terrains also differed erefore the re-sults in this paper were adapted to only relatively flat desertareas Additionally rainfall episodes with different in-tensities had different effects on the VWC and thermal

parameters as shown by field testing in the Loess Plateau[46] which is in agreement with the results in this paperHowever there was no notable wet layer in the studieddesert area

It is generally acknowledged that the soil color androughness length do not experience significant dynamicchanges thus the surface albedo depends on the solar el-evation angle and VWC e variation in albedo during therainfall episodes indicated that the short-term rainfall epi-sode in the desert area had little effect on the surface albedo

R2 = 065y = 062x ndash 229

500

300

100

ndash100500100ndash100

Hs +

LE

(Wmiddotm

ndash2)

Rn-G (Wmiddotmndash2)300

(a)

R2 = 064y = 067x ndash 179

500

300

100


Hs +

LE

(Wmiddotm

ndash2)

Rn-G-S (Wmiddotmndash2)300

(b)

R2 = 084y = 050x ndash 668

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(c)

R2 = 086y = 056x ndash 370

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(d)

Figure 10 Variations in the EBR before and after rainfall (a) without S before rainfall (b) with S before rainfall (c) without S after rainfall(d) with S after rainfall

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(a)

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(b)

Figure 11 EBR variation trends during the entire observation period (a) without S and (b) with S


because the clear day solar radiation was intense and theevaporation potential was very largee latter phenomenonresulted in the VWC rapidly evaporating out of the layerclosest to the surface in this area

A possible reason for the rapid increase in the VWC afterrainfall and the decreased growth rate from the shallow layerto the deep layers mentioned earlier was the infiltration ofrainwater after rainfall Although the VWC in the shallowlayer gradually decreased with an increase in solar radiationafter the sky cleared up the sandy soil surface easily formed ahardened layer leading to a reduction in the shallow soilporosity is porosity reduction caused the liquid water inthe subsoil to evaporate slowly e soil thermal capacityserves as an indicator of the degree of change in the ST andthe thermal capacity varies greatly with different soilcomponents consequently there are notable differences inthe thermal capacities of soils with different compositionse greater the thermal capacity the slower the ST changethis phenomenon is commonly known as cold soil andoccurs in sticky soil while the opposite phenomenon iscalled hot soil and occurs in light sandy soil e soil heatflux calculations at observation depths of 5 and 20 cm werebased mainly on shallow soil Similarly the soil heat capacitywas considered to be equal at depths of 0ndash20 cm while thevalue of S was calculated It is common to replace thethermal capacity of the layer above 5 cm with those of thelayers at depths of 5ndash20 cm In the desert area the soil in theshallow layer was dry while the change in the subsoilmoisture was more profound erefore the proposedmethod needs to be further improved and researched in thestudied desert area

e soil thermal conductivity represents the soil heattransfer performance and constitutes the basic physicalparameter for studying coupled hydrothermal motions onland surfaces e soil thermal conductivity dependedmainly on the VWC tightness and porosity Generallylight soil was better than sticky soil in terms of the thermalconductivity With an increase in the VWC the thermalconductivity was enhanced as a result the soil thermalconductivity clearly increased after rainfall in this papere soil particles in the desert were small resulting inintense water absorption and a poor water permeability ofthe soil erefore during both short-term heavy rainfalland systematic persistent precipitation the responses ofthe STand VWC in the shallow layer were more rapid thanthose in the deeper layers However the impact durationtime was short which led to results that are consistentwith the results reported by other domestic scholarsHowever due to differing soil properties the effects ofrainfall on the soil at different depths terrains ST andVWC values and soil thermal parameters were not thesame In this experiment a sandy soil density was usedbefore and after rainfall because the exact soil density hadnot been measured which may have had a certain effect onthe EBR calculations In addition the vegetation type andcoverage also affected the aforementioned parameterserefore there are still several remaining issues worthyof exploration

5 Conclusions

In this paper the effects of rainfall episodes on the surfacealbedo soil thermal parameters and EBR in the Badain JaranDesert were analyzed the results of this investigation are thekey to improving the parameterization of the surface ra-diation budget and energy balance for numerical models insemiarid areas In summary several characteristic obser-vations were made as follows

(1) Short-term rainfall had a large influence on the STand VWC compared with systematic precipitatione VWC increased rapidly after rainfall with adecreased growth rate from the shallow layer to thedeep layers e TCR in the shallow layer notablydecreased after rainfall and increased in the deeplayers e surface albedo during the short-termrainfall episode was significantly reduced andexhibited little change before and after rainfall esolar elevation angle had little effect on the surfacealbedo before and after rainfall instead the surfacealbedo was related to the smooth underlying desertsurface

(2) e soil thermal conductivity clearly increasedafter rainfall e water-free soil thermal con-ductivity followed the same trend that was relatedto the decreased porosity caused by the hardenedlayer which easily formed in the sandy soil surfaceafter rainfall and by the slower evaporation of theliquid water in the subsoil relative to the water atthe surface With an increasing VWC the soilthermal capacity thermal diffusivity and thermalconductivity slowly increased after rainfall Froma vertical depth perspective the soil thermalconductivity growth rate in the middle layer waslarger than that in the shallow layer before andafter rainfall similar trends were observed for thethermal diffusivity

(3) e diurnal variation curve of the global solar ra-diation was relatively smooth before rainfall and thedaily extremes reached nearly 1000Wmiddotmminus 2 e soilheat flux in each layer exhibited distinct diurnalvariations resembling quasisinusoids e fluctua-tion in the soil heat flux gradually decreased withincreasing depth and increased in each layer afterrainfall e change in the soil heat flux in the middlelayer lagged by approximately 4 h compared to thatin the shallow layer

(4) e EBR without S was 062 before rainfall butdecreased to 050 after rainfall Regardless of theoccurrence of rainfall the EBR with S increased byapproximately 5-6 however the EBR was stilllower after rainfall than before roughout theentire observation period the EBR in the daytimereached a maximum at approximately 1-2 days be-fore or after rainfall and gradually declined at othertimes


Data Availability

e observation data used to support the findings of thisstudy were supplied by the National Natural ScienceFoundation of China (41505008 and 41675020) underlicense and so cannot be made freely available Requests foraccess to these data should be made to Zhaoguo Li (zglilzbaccn)

Conflicts of Interest

e authors declare that they have no conflicts of interest

Acknowledgments

is research was funded by the National Natural ScienceFoundation of China (41875023 41505008 41675020 and41575008) and the China Special Fund for MeteorologicalResearch in the Public Interest (GYHY201506001-04 andGYHY201306066)

References

[1] J W Raich and A Tufekciogul ldquoVegetation and soil respi-ration correlations and controlsrdquo Biogeochemistry vol 48no 1 pp 71ndash90 2000

[2] D Gaumont-Guay T A Black T J Griffis et al ldquoInter-preting the dependence of soil respiration on soil temperatureand water content in a boreal aspen standrdquo Agricultural andForest Meteorology vol 140 no 1ndash4 pp 220ndash235 2006

[3] A Haines ldquoClimate change 2001 the scientific basis Con-tribution of working group 1 to the third assessment report ofthe intergovernmental panel on climate changerdquo In-ternational Journal of Epidemiology vol 32 no 2 p 321 2003

[4] V Sridhar W T A Jaksa B Fang et al ldquoEvaluating bias-corrected AMSR-E soil moisture using in situ observationsand model estimatesrdquo Vadose Zone Journal vol 12 no 3pp 1712ndash1717 2013

[5] W T Jaksa and V Sridhar ldquoEffect of irrigation in simulatinglong-term evapotranspiration climatology in a human-dominated river basin systemrdquo Agricultural and Forest Me-teorology vol 200 pp 109ndash118 2015

[6] Y Gao G Cheng W Liu et al ldquoModification of the soilcharacteristic parameters in Heihe River basin and effects onsimulated atmospheric elementsrdquo Plateau Meteorology vol 5no 8 2007 in Chinese

[7] Y Gao W Liu G Cheng H Peng H Li and Y Ran ldquoSetupand validation of the soil texture type distribution data in theHeihe River basinrdquo Plateau Meteorology vol 26 no 5pp 967ndash974 2007 in Chinese

[8] M F Wilson A Henderson-Sellers R E Dickinson andP J Kennedy ldquoSensitivity of the biosphere-atmospheretransfer scheme (BATS) to the inclusion of variable soilcharacteristicsrdquo Journal of Climate and Applied Meteorologyvol 26 no 3 pp 341ndash362 1987

[9] Q Zhang ldquoSimple review of land surface process modelrdquoScientiaMeteorologica Sinica vol 18 no 3 pp 295ndash304 1998in Chinese

[10] L Gan X Peng S Peth and R Horn ldquoEffects of grazingintensity on soil thermal properties and heat flux underLeymus chinensis and Stipa grandis vegetation in InnerMongolia Chinardquo Soil and Tillage Research vol 118pp 147ndash158 2012

[11] S Park J J Feddema and S L Egbert ldquoImpacts of hydrologicsoil properties on drought detection with MODIS thermaldatardquo Remote Sensing of Environment vol 89 no 1pp 53ndash62 2004

[12] F Wang J L Dufresne C Frederique and D Agnes ldquoeeffects of soil vertical discretization soil thermal propertiesand soil heat convection by liquid water transfer on the waterand energy cycles in a coupled land-atmosphere modelrdquoGeophysical Research vol 17 2015

[13] B P Guillod B Orlowsky D Miralles et al ldquoSoil moisture-precipitation coupling observations question an impact onprecipitation occurrence in North Americardquo Proceedings ofEuropean Geosciences Union General Assembly vol 15 2013

[14] B M Lofgren ldquoSensitivity of land-ocean circulations pre-cipitation and soil moisture to perturbed land surface al-bedordquo Journal of Climate vol 8 pp 2521ndash2542 2009

[15] J Otterman ldquoEnhancement of surface-atmosphere fluxes bydesert-fringe vegetation through reduction of surface albedoand of soil heat fluxrdquo eoretical amp Applied Climatologyvol 40 no 1-2 pp 67ndash79 1989

[16] V Sridhar and D A Wedin ldquoHydrological behaviour ofgrasslands of the Sandhills of Nebraska water and energy-balance assessment from measurements treatments andmodellingrdquo Ecohydrology vol 2 no 2 pp 195ndash212 2009

[17] V Sridhar K G Hubbard and D A Wedin ldquoAssessment ofsoil moisture dynamics of the Nebraska Sandhills using Long-Term measurements and a hydrology modelrdquo Journal of Ir-rigation and Drainage Engineering vol 132 no 5 pp 463ndash473 2006

[18] Q Zhang W Guoan S Wang and X Hou ldquoVertical changeof the soil structure parameters and the soil thermodynamicpara meters in the Gobi deserts in arid areasrdquo Arid ZoneResearch vol 20 no 1 pp 44ndash52 2003 in Chinese

[19] Q Zhang and Y Hu ldquoe flux-profile relationships under thecondition of heat advection over moist surfacerdquo ScientiaAtmospherica Sinica vol 19 no 1 1995 in Chinese

[20] Y Hu and Y Gao ldquoSome new understandings of processes atthe land surface in arid area from the HEIFErdquo Acta Mete-orologica Sinica vol 52 no 3 pp 285ndash296 1994 in Chinese

[21] Y Hu ldquoPreliminary analysis about characteristics of micro-climate and heat energy budget in HEXI GOBIrdquo PlateauMeteorology vol 9 no 2 pp 113ndash119 1990 in Chinese

[22] Q Zhang and X Cao ldquoe influence of synoptic conditionson the averaged surface heat and radiation budget energy overdesert or Gobirdquo Chinese Journal of Atmospheric Sciencesvol 27 no 2 pp 245ndash254 2003 in Chinese

[23] Z Yang X Li Y SUN L Liu X Zhang and Y MaldquoCharacteristics of rainfall interception and stemflow for Salixpsammophila in Maowusu sandland Northwest ChinardquoAdvances inWater Science vol 19 no 5 pp 693ndash698 2008 inChinese

[24] J You K G Hubbard R Mahmood V Sridhar andD Todey ldquoQuality control of soil water data in applied climateinformation system-case study in Nebraskardquo Journal of Hy-drologic Engineering vol 15 no 3 pp 200ndash209 2010

[25] K G Hubbard J You V Sridhar E Hunt S Korner andG Roebke ldquoNear-surface soil-water monitoring for waterresources in management on a wide-area basis in the GreatPlainsrdquo Great Plains Research vol 19 no 1 pp 45ndash54 2009

[26] V Sridhar ldquoTracking the influence of irrigation on landsurface fluxes and boundary layer climatologyrdquo Journal ofContemporary Water Research amp Education vol 152 no 1pp 79ndash93 2013


[27] V Sridhar and K G Hubbard ldquoEstimation of the waterbalance using observed soil water in the Nebraska SandhillsrdquoJournal of Hydrologic Engineering vol 15 no 1 pp 70ndash782010

[28] Q He andM Xiang ldquoAnalyzed on a heavy precipitation in thehinterland of Taklimakan desertrdquo Arid Zone Research vol 15no 1 pp 15ndash20 1998 in Chinese

[29] Z Yang W Chen G Chen and Z Dong ldquoCharacteristics ofthe weather in the hinterland of the Taklimakan desertrdquoJournal of Desert Research vol 15 no 3 pp 293ndash298 1995 inChinese

[30] D Sun and J Yang ldquoPrecipitation characteristics at thehinterland of Gurbantunggut desert and the surroundingareasrdquo Arid Land Geography vol 33 no 5 pp 769ndash774 2010in Chinese

[31] K Zhang Z Yao Z An and S Xie ldquoWind-blown sandenvironment precipitation over the Badain Jaran Desert andits adjacent regionsrdquo Journal of Desert Research vol 32 no 5pp 442ndash466 2012 in Chinese

[32] J Zhu N A Wang H B Chen C Y Dong and H A ZhangldquoStudy on the boundary and the area of Badain Jaran Desertbased on remote sensing imageryrdquo Progress in Geographyvol 29 no 9 pp 1087ndash1094 2010 in Chinese

[33] N Ma and X Yang ldquoEnvironmental isotopes and waterchemistry in the Badain Jaran Desert and in its southeasternadjacent areas inner Mongolia and their hydrological im-plicationsrdquo Quaternary Sciences vol 28 no 4 pp 702ndash7112008 in Chinese

[34] D A Haugen J C Kaimal and E F Bradley ldquoAn experi-mental study of Reynolds stress and heat flux in the atmo-spheric surface layerrdquo Quarterly Journal of the RoyalMeteorological Society vol 97 no 412 pp 168ndash180 2010

[35] Z Qiang and H Ronghui ldquoParameters of land-surface pro-cesses for Gobi in north-west Chinardquo Boundary-Layer Me-teorology vol 110 no 3 pp 471ndash478 2004

[36] K Yang and J Wang ldquoA temperature prediction correctionmethod for calculating surface soil heat flux based on soiltemperature and humidity datardquo Science In China Pressvol 38 no 2 pp 243ndash250 2008 in Chinese

[37] J P Peixoto and A H Oort ldquoPhysics of climaterdquo Reviews ofModern Physics vol 56 no 365 1984

[38] Q Zhang R Huang S WangW Guoan X Cao and X HouldquoNWC-ALIEX and its research advancesrdquo Advances In EarthScience vol 20 no 4 pp 427ndash441 2005

[39] H Liu B Wang and C Fu ldquoRelationships between surfacealbedo soil thermal parameters and soil moisture in the semi-arid area of Tongyu northeastern Chinardquo Advances in At-mospheric Sciences vol 25 no 5 pp 757ndash764 2008

[40] Z Liu G Tu and W Dong ldquoe variation characteristics ofalbedo in different surface of semi-arid regionrdquo Science inChina Press vol 53 no 10 pp 1220ndash1227 2008 in Chinese

[41] Y Liu Q He H Zhang and M Ali ldquoStudies of land-at-mosphere interaction parameters in Taklimakan Deserthinterlandrdquo Plateau Meteorology vol 30 no 5 pp 1294ndash1299 2011 in Chinese

[42] Q Zhang X Cao G Wei and R Huang ldquoObservation andstudy of land surface parameters over Gobi in typical aridregionrdquo Advances in Atmospheric Sciences vol 19 no 1pp 121ndash135 2002

[43] B G Heusinkveld A F G Jacobs A A M Holtslag andS M Berkowicz ldquoSurface energy balance closure in an aridregion role of soil heat fluxrdquo Agricultural and Forest Mete-orology vol 122 no 1-2 pp 21ndash37 2004

[44] J Li Y Ao and Z Li ldquoComparative analysis of radiation andenergy budget over Badain Jaran Desert on clear and cloudydays in summerrdquo Progress in Geography vol 31 no 11pp 1443ndash1451 2012 in Chinese

[45] N Wang N Ma H B Chen X L Chen C Y Dong andZ Y Zhang ldquoA preliminary study of precipitation charac-teristics in the hinterland of Badain Jaran DesertrdquoAdvances inWater Science vol 24 no 2 pp 2153ndash2160 2013 in Chinese

[46] P Yue Q Zhang J Yang et al ldquoSurface heat flux and energybudget for semi-arid grassland on the Loess Plateaurdquo ActaEcologica Sinica vol 31 no 22 pp 6866ndash6876 2011 inChinese


Hindawiwwwhindawicom Volume 2018

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Applied ampEnvironmentalSoil Science

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Journal of




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AgricultureAdvances in


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MeteorologyAdvances in

Hindawi Publishing Corporation httpwwwhindawicom Volume 2013Hindawiwwwhindawicom

The Scientific World Journal

Volume 2018Hindawiwwwhindawicom Volume 2018

ChemistryAdvances in

ScienticaHindawiwwwhindawicom Volume 2018


Geological ResearchJournal of

Analytical ChemistryInternational Journal of


Submit your manuscripts atwwwhindawicom

thermal properties and heat fluxes of soil using a variety ofmethods and products [10ndash15] including the NOAH LandSurface Model (LSM) for estimating net radiation and latentsensible and ground heat (GH) fluxes as well as waterbalance components in four land treatments [16] a hy-drological model for the simulation of soil moisture acrossmultiple depths [17]

e majority of arid regions in Northwest China aredesert or Gobi and are subject to intense solar radiation as aresult the soil parameters are vastly different from those oftypical regions and the land surface physical processestherein exhibit notable regional characteristics [18] Sincethe late 1980s comprehensive field experiments have beencarried out on land surface processes e Heihe River fieldexperiment (HEIFE) and the field experiment on the air-land interaction in the arid area of Northwest China (NWC-ALIEX) have confirmed certain soil parameters in the soilsurface of their research regions [19ndash22] However com-paratively speaking specific research on the soil parametersin arid regions is still limited

As the main water source in desert areas precipitationhas a considerable impact on themovement of dunes and thedistribution of vegetation [23ndash27] Due to limitations posedby the natural environment only a small number of ob-servation stations with an uneven spatial distribution aresituated in the arid desert area of Northwest China as aresult the characteristics of the soil physical parameterstherein specifically in the untraversed desert hinterlands arepoorly understood Nevertheless local meteorologists haveconducted a large amount of research in the Taklamakan andGurbantunggut Deserts and their work has resulted innumerous achievements with regard to the effects of pre-cipitation on deserts and their surrounding areas [28ndash30]

e Badain Jaran Desert is host to a variety of wavylandforms and sand mountains the latter of which are thehighest in the world and these landforms have profoundeffects on rainfall Zhang et al analyzed the rainfall distri-bution in this region based on data from meteorologicalstations located around the desert [31] However few studieshave investigated the effects of rainfall on the thermalproperties of soil in deserts

In this paper hourly rainfall data acquired during theintense observation period (IOP hereinafter) in the BadainJaran Desert hinterland were integrated Basic data in-cluding the surface sensible heat flux latent heat flux andshallow soil thermal storage data were obtained and thesurface albedo soil volumetric heat capacity thermal con-ductivity thermal diffusivity and energy balance ratio (EBR)were calculated by relevant equationse effects of differenttypes of rainfall on these soil characteristics and on thesurface energy balances were analyzed the results of whichreveal the energy and water distributions in the underlyingsurface layer throughout the arid region of Northwest China

2 Materials and Methods

21 Materials e Badain Jaran Desert located in the AlxaBanner of Inner Mongolia at approximately 395degndash42degN and985degndash104degE is the second-largest desert in China with an

area of approximately 52000 square kilometers [32] isdesert is mainly influenced by westerlies namely the Indianand East Asian monsoons and belongs to temperate aridand extremely arid climate zones e average annualprecipitation exhibits a decreasing trend from the southeast(approximately 120mm) to the northwest (less than 40mm)[33] precipitation primarily occurs from July to Augustenorthwest arid area which is subject to a large amount ofevaporation and abundant sunshine is sensitive to climatechange and possesses a fragile ecological environmentHence the northwest arid area is considered an ideal site toobserve the water and heat exchanges in the underlyingdesert surface

From June to September of 2009 researchers carried outa series of field observation experiments in the hinterland ofthe Badain Jaran Deserte observation points were locatedin the southeast of the desert (39deg28122primeN and 102deg22365primeEat an altitude of 1418m)e D1 observation site which wassurrounded by an open undulating yellow sand terrain is acharacteristic desert area Sparse vegetation was distributedapproximately 500sim700m from the observational stationmost of which was Alhagi sparsifolia and Nitraria tangu-torum Bobr was also present (as shown in Figure 1)

e air temperature and humidity wind precipitationsoil temperature (ST hereinafter) and soil moisture (volu-metric water content VWC hereinafter) land surface ra-diation and turbulence were observed e IOP lasted fromJune 21st to September 12th In this paper the local standardtime (LST hereinafter) which was 7 h ahead of CoordinatedUniversal Time (UTC) was selected for the calculation andanalysis

e data from August 4th to September 20th were se-lected for analysis to reflect the effects of rainfall on the soilthermal properties and energy balances in the desert hin-terland During this period there were two large-scaleprecipitation events one occurred on August 18th with29mm of precipitation and the other occurred on September5ndash7th with 226mm of total precipitation ese eventsrepresent rare phenomena in this extremely arid desert area

22 Methods e hourly precipitation distributions of thetwo aforementioned synoptic processes are shown in Fig-ure 2 which shows that the first weather event (August 18th)had a short precipitation duration with a high intensity themaximum rainfall intensity reached 78mmmiddothminus 1 In contrastthe second weather event had a longer duration but themaximum intensity was only 28mmmiddothminus 1 is result in-dicates that the two precipitation processes were notablydifferent the first weather event was an extremely intenserainfall episode the sort of which is typical in the arid regionof Northwest China while the second weather event wascharacteristic of systematic rainfall

e sampling frequency of the surface turbulence datawas 10Hz while the radiometer and soil heat flux plategenerated average ST and VWC values respectively every30min Basic data quality control measures such as outlierelimination time delay correction virtual temperature cor-rection and WebbndashPearmanndashLeuning (WPL) correction









cs G1 minus G2

Δzlowast zTgzt1113872 1113873 (3)


Δzlowast zTgzt1113872 1113873 (4)

Gansu

Qinghai

InnerMongolia

NingxiaEjina Qi

Guaizi lake

Bayinnuorigong

Alxa Right Banner

D1

Zhangye

Gaotai

Dingxin

Jinta

0 35 70 140 210Km

N


39degN

40degN

41degN

42degN




90

80

70

60

50

40

30

20

10

00

(Aug 18)TimeLST

Prec

ipita

tion

(mm

)

0000 0200 0400 0600 0800 1000

(a)

30

20

10

000000 0800 1600 0000 0800 1600 0000


Prec

ipita

tion

(mm

)

(b)



λsi Gi

zTgzz (5)

Ksi λsiCs

(6)



Gsfc Gz + S (7)

S 1113946zzref


zT

ztdz (8)




α RSU

RSD (10)

EBR 1113936(H + LE)



3 Results














012

010

008

006

004

002

(a)

(b)4030201000


Date

5cm10cm

20cm40cm


Soil_

VW

C (m

3 middotmndash3

)So

il_TC

R (deg

Cmiddothndash1

)






Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time

20cm40cm

Air5cm10cm

0000 0400 0800 1200 1600 2000 2400

(a)

20cm40cm

Air5cm10cm

Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time0000 0400 0800 1200 1600 2000 2400

(b)


06

05

04

03

02

Alb

edo

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

(a)

06

05

04

03

0210 20 30 40 50 60 70

Alb

edo


(b)





R2 = 086y = 109x + 108

100

50

0

ndash50


∆G (W

middotmndash2

)

ndash50 0 50 100

(a)

120

60

0


R2 = 093y = 154x + 024


∆G (W

middotmndash2

)

(b)

100

50

0

ndash50

R2 = 084y = 098x + 107

∆G (W

middotmndash2

)


(c)

R2 = 090y = 125x + 021

100

50

0

ndash50

∆G (W

middotmndash2

)


(d)


30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(a)

30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(b)








R2 = 085y = 023x + 1352

100

70

40

10

ndash20

ndash50


G5 (

Wmiddotm

ndash2)


(a)

200

150

100

50

0

ndash50

ndash100


R2 = 086y = 066x + 264


G5 (

Wmiddotm

ndash2)

(b)

R2 = 068y = 031x + 050

20

10

0



G20

(Wmiddotm

ndash2)

(c)

50

30

10

ndash10

ndash30

R2 = 095y = 145x ndash 010


G20

(Wmiddotm

ndash2)

(d)









Global radiation

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

5cm20cm

Glo

bal r

adia

tion

(Wmiddotm

ndash2)

Soil

heat

flux

(Wmiddotm

ndash2)

1200 (a)

(b)

1000

800

600

400

200

0

150

100

50

0

ndash50

ndash100



4 Discussion




R2 = 065y = 062x ndash 229

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(a)

R2 = 064y = 067x ndash 179

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(b)

R2 = 084y = 050x ndash 668

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(c)

R2 = 086y = 056x ndash 370

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(d)


16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(a)

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(b)






5 Conclusions







Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy






















cs G1 minus G2

Δzlowast zTgzt1113872 1113873 (3)


Δzlowast zTgzt1113872 1113873 (4)

Gansu

Qinghai

InnerMongolia

NingxiaEjina Qi

Guaizi lake

Bayinnuorigong

Alxa Right Banner

D1

Zhangye

Gaotai

Dingxin

Jinta

0 35 70 140 210Km

N


39degN

40degN

41degN

42degN




90

80

70

60

50

40

30

20

10

00

(Aug 18)TimeLST

Prec

ipita

tion

(mm

)

0000 0200 0400 0600 0800 1000

(a)

30

20

10

000000 0800 1600 0000 0800 1600 0000


Prec

ipita

tion

(mm

)

(b)



λsi Gi

zTgzz (5)

Ksi λsiCs

(6)



Gsfc Gz + S (7)

S 1113946zzref


zT

ztdz (8)




α RSU

RSD (10)

EBR 1113936(H + LE)



3 Results














012

010

008

006

004

002

(a)

(b)4030201000


Date

5cm10cm

20cm40cm


Soil_

VW

C (m

3 middotmndash3

)So

il_TC

R (deg

Cmiddothndash1

)






Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time

20cm40cm

Air5cm10cm

0000 0400 0800 1200 1600 2000 2400

(a)

20cm40cm

Air5cm10cm

Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time0000 0400 0800 1200 1600 2000 2400

(b)


06

05

04

03

02

Alb

edo

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

(a)

06

05

04

03

0210 20 30 40 50 60 70

Alb

edo


(b)





R2 = 086y = 109x + 108

100

50

0

ndash50


∆G (W

middotmndash2

)

ndash50 0 50 100

(a)

120

60

0


R2 = 093y = 154x + 024


∆G (W

middotmndash2

)

(b)

100

50

0

ndash50

R2 = 084y = 098x + 107

∆G (W

middotmndash2

)


(c)

R2 = 090y = 125x + 021

100

50

0

ndash50

∆G (W

middotmndash2

)


(d)


30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(a)

30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(b)








R2 = 085y = 023x + 1352

100

70

40

10

ndash20

ndash50


G5 (

Wmiddotm

ndash2)


(a)

200

150

100

50

0

ndash50

ndash100


R2 = 086y = 066x + 264


G5 (

Wmiddotm

ndash2)

(b)

R2 = 068y = 031x + 050

20

10

0



G20

(Wmiddotm

ndash2)

(c)

50

30

10

ndash10

ndash30

R2 = 095y = 145x ndash 010


G20

(Wmiddotm

ndash2)

(d)









Global radiation

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

5cm20cm

Glo

bal r

adia

tion

(Wmiddotm

ndash2)

Soil

heat

flux

(Wmiddotm

ndash2)

1200 (a)

(b)

1000

800

600

400

200

0

150

100

50

0

ndash50

ndash100



4 Discussion




R2 = 065y = 062x ndash 229

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(a)

R2 = 064y = 067x ndash 179

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(b)

R2 = 084y = 050x ndash 668

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(c)

R2 = 086y = 056x ndash 370

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(d)


16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(a)

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(b)






5 Conclusions







Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy















λsi Gi

zTgzz (5)

Ksi λsiCs

(6)



Gsfc Gz + S (7)

S 1113946zzref


zT

ztdz (8)




α RSU

RSD (10)

EBR 1113936(H + LE)



3 Results














012

010

008

006

004

002

(a)

(b)4030201000


Date

5cm10cm

20cm40cm


Soil_

VW

C (m

3 middotmndash3

)So

il_TC

R (deg

Cmiddothndash1

)






Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time

20cm40cm

Air5cm10cm

0000 0400 0800 1200 1600 2000 2400

(a)

20cm40cm

Air5cm10cm

Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time0000 0400 0800 1200 1600 2000 2400

(b)


06

05

04

03

02

Alb

edo

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

(a)

06

05

04

03

0210 20 30 40 50 60 70

Alb

edo


(b)





R2 = 086y = 109x + 108

100

50

0

ndash50


∆G (W

middotmndash2

)

ndash50 0 50 100

(a)

120

60

0


R2 = 093y = 154x + 024


∆G (W

middotmndash2

)

(b)

100

50

0

ndash50

R2 = 084y = 098x + 107

∆G (W

middotmndash2

)


(c)

R2 = 090y = 125x + 021

100

50

0

ndash50

∆G (W

middotmndash2

)


(d)


30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(a)

30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(b)








R2 = 085y = 023x + 1352

100

70

40

10

ndash20

ndash50


G5 (

Wmiddotm

ndash2)


(a)

200

150

100

50

0

ndash50

ndash100


R2 = 086y = 066x + 264


G5 (

Wmiddotm

ndash2)

(b)

R2 = 068y = 031x + 050

20

10

0



G20

(Wmiddotm

ndash2)

(c)

50

30

10

ndash10

ndash30

R2 = 095y = 145x ndash 010


G20

(Wmiddotm

ndash2)

(d)









Global radiation

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

5cm20cm

Glo

bal r

adia

tion

(Wmiddotm

ndash2)

Soil

heat

flux

(Wmiddotm

ndash2)

1200 (a)

(b)

1000

800

600

400

200

0

150

100

50

0

ndash50

ndash100



4 Discussion




R2 = 065y = 062x ndash 229

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(a)

R2 = 064y = 067x ndash 179

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(b)

R2 = 084y = 050x ndash 668

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(c)

R2 = 086y = 056x ndash 370

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(d)


16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(a)

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(b)






5 Conclusions







Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy





















012

010

008

006

004

002

(a)

(b)4030201000


Date

5cm10cm

20cm40cm


Soil_

VW

C (m

3 middotmndash3

)So

il_TC

R (deg

Cmiddothndash1

)






Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time

20cm40cm

Air5cm10cm

0000 0400 0800 1200 1600 2000 2400

(a)

20cm40cm

Air5cm10cm

Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time0000 0400 0800 1200 1600 2000 2400

(b)


06

05

04

03

02

Alb

edo

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

(a)

06

05

04

03

0210 20 30 40 50 60 70

Alb

edo


(b)





R2 = 086y = 109x + 108

100

50

0

ndash50


∆G (W

middotmndash2

)

ndash50 0 50 100

(a)

120

60

0


R2 = 093y = 154x + 024


∆G (W

middotmndash2

)

(b)

100

50

0

ndash50

R2 = 084y = 098x + 107

∆G (W

middotmndash2

)


(c)

R2 = 090y = 125x + 021

100

50

0

ndash50

∆G (W

middotmndash2

)


(d)


30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(a)

30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(b)








R2 = 085y = 023x + 1352

100

70

40

10

ndash20

ndash50


G5 (

Wmiddotm

ndash2)


(a)

200

150

100

50

0

ndash50

ndash100


R2 = 086y = 066x + 264


G5 (

Wmiddotm

ndash2)

(b)

R2 = 068y = 031x + 050

20

10

0



G20

(Wmiddotm

ndash2)

(c)

50

30

10

ndash10

ndash30

R2 = 095y = 145x ndash 010


G20

(Wmiddotm

ndash2)

(d)









Global radiation

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

5cm20cm

Glo

bal r

adia

tion

(Wmiddotm

ndash2)

Soil

heat

flux

(Wmiddotm

ndash2)

1200 (a)

(b)

1000

800

600

400

200

0

150

100

50

0

ndash50

ndash100



4 Discussion




R2 = 065y = 062x ndash 229

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(a)

R2 = 064y = 067x ndash 179

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(b)

R2 = 084y = 050x ndash 668

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(c)

R2 = 086y = 056x ndash 370

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(d)


16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(a)

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(b)






5 Conclusions







Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy


















Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time

20cm40cm

Air5cm10cm

0000 0400 0800 1200 1600 2000 2400

(a)

20cm40cm

Air5cm10cm

Air_

Soil_

TCR

(degCmiddot

hndash1)

2

1

0

ndash1

ndash2

ndash3

ndash4

Time0000 0400 0800 1200 1600 2000 2400

(b)


06

05

04

03

02

Alb

edo

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

(a)

06

05

04

03

0210 20 30 40 50 60 70

Alb

edo


(b)





R2 = 086y = 109x + 108

100

50

0

ndash50


∆G (W

middotmndash2

)

ndash50 0 50 100

(a)

120

60

0


R2 = 093y = 154x + 024


∆G (W

middotmndash2

)

(b)

100

50

0

ndash50

R2 = 084y = 098x + 107

∆G (W

middotmndash2

)


(c)

R2 = 090y = 125x + 021

100

50

0

ndash50

∆G (W

middotmndash2

)


(d)


30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(a)

30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(b)








R2 = 085y = 023x + 1352

100

70

40

10

ndash20

ndash50


G5 (

Wmiddotm

ndash2)


(a)

200

150

100

50

0

ndash50

ndash100


R2 = 086y = 066x + 264


G5 (

Wmiddotm

ndash2)

(b)

R2 = 068y = 031x + 050

20

10

0



G20

(Wmiddotm

ndash2)

(c)

50

30

10

ndash10

ndash30

R2 = 095y = 145x ndash 010


G20

(Wmiddotm

ndash2)

(d)









Global radiation

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

5cm20cm

Glo

bal r

adia

tion

(Wmiddotm

ndash2)

Soil

heat

flux

(Wmiddotm

ndash2)

1200 (a)

(b)

1000

800

600

400

200

0

150

100

50

0

ndash50

ndash100



4 Discussion




R2 = 065y = 062x ndash 229

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(a)

R2 = 064y = 067x ndash 179

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(b)

R2 = 084y = 050x ndash 668

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(c)

R2 = 086y = 056x ndash 370

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(d)


16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(a)

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(b)






5 Conclusions







Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy

















R2 = 086y = 109x + 108

100

50

0

ndash50


∆G (W

middotmndash2

)

ndash50 0 50 100

(a)

120

60

0


R2 = 093y = 154x + 024


∆G (W

middotmndash2

)

(b)

100

50

0

ndash50

R2 = 084y = 098x + 107

∆G (W

middotmndash2

)


(c)

R2 = 090y = 125x + 021

100

50

0

ndash50

∆G (W

middotmndash2

)


(d)


30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(a)

30

25

20

15

10

05

00

Soil

ther

mal

capa

city

(106 Jmiddotm

ndash3middotK

ndash1)


(b)








R2 = 085y = 023x + 1352

100

70

40

10

ndash20

ndash50


G5 (

Wmiddotm

ndash2)


(a)

200

150

100

50

0

ndash50

ndash100


R2 = 086y = 066x + 264


G5 (

Wmiddotm

ndash2)

(b)

R2 = 068y = 031x + 050

20

10

0



G20

(Wmiddotm

ndash2)

(c)

50

30

10

ndash10

ndash30

R2 = 095y = 145x ndash 010


G20

(Wmiddotm

ndash2)

(d)









Global radiation

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

5cm20cm

Glo

bal r

adia

tion

(Wmiddotm

ndash2)

Soil

heat

flux

(Wmiddotm

ndash2)

1200 (a)

(b)

1000

800

600

400

200

0

150

100

50

0

ndash50

ndash100



4 Discussion




R2 = 065y = 062x ndash 229

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(a)

R2 = 064y = 067x ndash 179

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(b)

R2 = 084y = 050x ndash 668

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(c)

R2 = 086y = 056x ndash 370

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(d)


16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(a)

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(b)






5 Conclusions







Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy




















R2 = 085y = 023x + 1352

100

70

40

10

ndash20

ndash50


G5 (

Wmiddotm

ndash2)


(a)

200

150

100

50

0

ndash50

ndash100


R2 = 086y = 066x + 264


G5 (

Wmiddotm

ndash2)

(b)

R2 = 068y = 031x + 050

20

10

0



G20

(Wmiddotm

ndash2)

(c)

50

30

10

ndash10

ndash30

R2 = 095y = 145x ndash 010


G20

(Wmiddotm

ndash2)

(d)









Global radiation

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

5cm20cm

Glo

bal r

adia

tion

(Wmiddotm

ndash2)

Soil

heat

flux

(Wmiddotm

ndash2)

1200 (a)

(b)

1000

800

600

400

200

0

150

100

50

0

ndash50

ndash100



4 Discussion




R2 = 065y = 062x ndash 229

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(a)

R2 = 064y = 067x ndash 179

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(b)

R2 = 084y = 050x ndash 668

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(c)

R2 = 086y = 056x ndash 370

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(d)


16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(a)

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(b)






5 Conclusions







Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy





















Global radiation

Date (d)08-12 08-14 08-16 08-18 08-20 08-22 08-24

5cm20cm

Glo

bal r

adia

tion

(Wmiddotm

ndash2)

Soil

heat

flux

(Wmiddotm

ndash2)

1200 (a)

(b)

1000

800

600

400

200

0

150

100

50

0

ndash50

ndash100



4 Discussion




R2 = 065y = 062x ndash 229

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(a)

R2 = 064y = 067x ndash 179

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(b)

R2 = 084y = 050x ndash 668

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(c)

R2 = 086y = 056x ndash 370

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(d)


16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(a)

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(b)






5 Conclusions







Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy















4 Discussion




R2 = 065y = 062x ndash 229

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(a)

R2 = 064y = 067x ndash 179

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(b)

R2 = 084y = 050x ndash 668

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(c)

R2 = 086y = 056x ndash 370

500

300

100


Hs +

LE

(Wmiddotm

ndash2)


(d)


16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(a)

16

12

08

04

00

EBR

Date (d)08-04 08-10 08-16 08-22 08-28 09-03 09-09 09-15 09-21

(b)






5 Conclusions







Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy


















5 Conclusions







Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy















Data Availability




Acknowledgments


References


















































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy





































Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy
















Journal of










Volume 2018





Geophysics


Journal of




Microbiology





Agronomy















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