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Sciences in Cold and Arid Regions ›› 2021, Vol. 13 ›› Issue (1): 18-29.doi: 10.3724/SP.J.1226.2021.20059

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Simulated effect of soil freeze-thaw process on surface hydrologic and thermal fluxes in frozen ground region of the Northern Hemisphere

Di Ma1,2,SiQiong Luo1(),DongLin Guo3,ShiHua Lyu4,1,XianHong Meng1,BoLi Chen5,LiHui Luo6   

  1. 1.Key Laboratory for Land Surface Process and Climate Change in Cold and Arid Regions, Northwest Institute of Eco-Environment and Resources, Chinese Academy of Science, Lanzhou, Gansu 730000, China
    2.College of Atmospheric Sciences, Lanzhou University, Lanzhou, Gansu 730000, China
    3.Nansen-Zhu International Research Center, Institute of Atmospheric Physics, Chinese Academy of Sciences, Beijing 100029, China
    4.School of Atmospheric Sciences, Plateau Atmosphere and Environment Key Laboratory of Sichuan Province, Chengdu University of Information Technology, Chengdu, Sichuan 610225, China
    5.Changzhou Meteorological Bureau, Changzhou, Jiangsu 213000, China
    6.State Key Laboratory of Frozen Soils Engineering, Northwest Institute of Eco-Environment and Resources, Chinese Academy of Sciences, Lanzhou, Gansu 730000, China
  • Received:2019-12-24 Accepted:2020-10-22 Online:2021-02-28 Published:2021-02-07
  • Contact: SiQiong Luo E-mail:lsq@lzb.ac.cn
  • Supported by:
    the National Nature Science Foundation of China(42075091);CAREERI STS Funding(Y651671001)

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Abstract:

Soil freeze-thaw process is closely related to surface energy budget, hydrological activity, and terrestrial ecosystems. In this study, two numerical experiments (including and excluding soil freeze-thaw process) were designed to examine the effect of soil freeze-thaw process on surface hydrologic and thermal fluxes in frozen ground region in the Northern Hemisphere based on the state-of-the-art Community Earth System Model version 1.0.5. Results show that in response to soil freeze-thaw process, the area averaged soil temperature in the shallow layer (0.0175-0.0451 m) decreases by 0.35 ℃ in the TP (Tibetan Plateau), 0.69 ℃ in CES (Central and Eastern Siberia), and 0.6 ℃ in NA (North America) during summer, and increases by 1.93 ℃ in the TP, 2.28 ℃ in CES and 1.61 ℃ in NA during winter, respectively. Meanwhile, in response to soil freeze-thaw process, the area averaged soil liquid water content increases in summer and decrease in winter. For surface heat flux components, the ground heat flux is most significantly affected by the freeze-thaw process in both summer and winter, followed by sensible heat flux and latent heat flux in summer. In the TP area, the ground heat flux increases by 2.82 W/m2 (28.5%) in summer and decreases by 3.63 W/m2 (40%) in winter. Meanwhile, in CES, the ground heat flux increases by 1.89 W/m2 (11.3%) in summer and decreases by 1.41 W/m2 (18.6%) in winter. The heat fluxes in the Tibetan Plateau are more susceptible to the freeze-thaw process compared with the high-latitude frozen soil regions. Soil freeze-thaw process can induce significant warming in the Tibetan Plateau in winter. Also, this process induces significant cooling in high-latitude regions in summer. The frozen ground can prevent soil liquid water from infiltrating to deep soil layers at the beginning of thawing; however, as the frozen ground thaws continuously, the infiltration of the liquid water increases and the deep soil can store water like a sponge, accompanied by decreasing surface runoff. The influence of the soil freeze-thaw process on surface hydrologic and thermal fluxes varies seasonally and spatially.

Key words: freeze-thaw effect, hydrologic and thermal, frozen ground, Northern Hemisphere

Figure 1

Differences between CTL and NSFT experiments (CTL-NSFT) of the soil ice (kg/m2) in three layers during JJA (left) and DJF (right): (a, b) shallow layer, (c, d) medium layer, and (e, f) deep layer. Yellow box indicates CES (Central and East Siberia); red box indicates NA (North America); red box indicates TP (Tibet Plateau). Colors indicate statistically significant changes (P <0.1)"

Figure 2

Differences between the CTL and NSFT (CTL-NSFT) experiments of the soil liquid water (m3/m3) in three layers during JJA (left) and DJF (right): (a, b) shallow layer, (c, d) medium layer, and (e, f) deep layer. Colors indicate statistically significant changes (P <0.1)"

Figure 3

Simulated differences between CTL and NSFT (CTL-NSFT) of the soil temperature and soil liquid water at three different depths, which are area averaged over three specific regions of (a1, a2, a3) NA, (b1, b2, b3) CES, and (c1, c2, b3) the TP"

Figure 4

Differences between the CTL and NSFT experiments of the soil temperature (℃) in three layers during JJA (left) and DJF (right): (a, b) shallow layer, (c, d) medium layer, and (e, f) deep layer. Colors indicate statistically significant changes (P <0.1)"

Table 1

Differences between the CTL and NSFT experiments (CTL-NSFT) for variables during the summer (JJA) and winter (DJF), averaged over the TP, CES and NA"

(CTL-NSFT)UnitJJADJF
TPCESNATPCESNA
Soil temperature (S)℃-0.350.69-0.601.932.281.61
Soil temperature (M)℃-0.72-1.85-1.302.292.461.76
Soil temperature (D)℃-1.81-1.68-1.273.322.631.80
2-m air temperature℃-0.14-0.44-0.451.57-0.29-0.10
Surface temperature℃-0.25-0.44-0.411.75-0.25-0.06
Net radiation fluxW/m2-0.097-0.843-1.626-0.849-1.114-0.045
Latent heatW/m2

0.32

(0.4%)

-0.42

(-0.8%)

-0.30

(-0.7%)

0.66

(5%)

0.12

(21.8%)

0.26

(14.9%)

Sensible heatW/m2

-3.21

(-7.5%)

-1.82

(-4.4%)

-2.53

(-7.1%)

2.10

(2.16%)

0.18

(1.1%)

0.62

(3.2%)

Ground heatW/m2

2.82

(28.5%)

1.89

(11.3%)

1.92

(13.5%)

-3.63

(-40.8%)

-1.41

(-18.6%)

-1.01

(-14.9%)

Figure 5

Differences between the CTL and NSFT (CTL-NSFT) experiments of the ground heat flux (a, b), sensible heat flux (c, d), ground source heat flux (e, f) and latent heat flux (g, h), (Unit: W/m2). Left column is in JJA; right column is in DJF. Colors indicate statistically significant changes (P <0.1)"

Figure 6

Simulated differences between CTL and NSFT (CTL-NSFT) of the energy budget components, including latent heat, sensible heat and ground heat, in the three specific regions of (a) NA, (b) CES, and (c) TP"

Figure 7

Simulated differences between CTL and NSFT (CTL-NSFT) of the water cycle components, including infiltration, runoff, precipitation, and evaporation, in the three specific regions of (a) NA, (b) CES, and (c) TP"

Figure 8

Simulated differences between CTL and NSFT (CTL-NSFT) in the vertical profiles of vertical motion, in the three specific regions of (a) NA, (b) CES, and (c) TP (Pa/s)"

Figure 9

Runoff (first row) and infiltration (second row) in CTL and NSFT simulations in three specific regions: (a, d) NA, (b, e) CES, and (c, f) the TP. For runoff, with the shaded area indicating that runoff in NSFT is larger than that in CTL; and infiltration, with the shaded area indicating that infiltration in CTL is larger than that in NSFT"

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