1. Introduction

The water and energy cycles on the Tibetan Plateau are related to the variations in the Asian monsoon (Reference WebsterWebster and others, 1998). Consequently, the uplifted land surface of the plateau, the anomaly of the area and duration of the snow cover influence the strength, onset and the end of the Asian monsoon (Reference Barnett, Dümenil, Schlese, Roeckner and LatifBarnett and others, 1989; Reference Yasunari, Kitoh and TokiokaYasunari and others, 1991; Reference Vernekar, Zhou and ShuklaVernekar and others, 1995). The Tibetan Plateau has profound dynamic and thermodynamic effects on the general atmospheric circulation and climate in East Asia, and especially in China. Reference Hahn and ManabeHahn and Manabe (1975) found that the Asian summer monsoon can be reasonably simulated only with the Tibetan Plateau topography incorporated into the GFL general circulation model. Reference WangWang (1984) and Reference Wu and ZhangWu and Zhang (1998) pointed out that the onset of the Asian monsoon depends to a large extent on the thermal effect of the plateau. Reference Kuo and QianKuo and Qian (1982) found the topography of the Tibetan Plateau has a profound effect on the simulated precipitation pattern. Reference Qian, Yian, Wang and WangQian and others (1988, Reference Qian, Wang and Shao2001, Reference Qian, Zheng, Zhang and Miao2003) discovered important influences of the plateau on rainfall and the onset date of the monsoon.

The snow anomaly over the Tibetan Plateau changes its thermal forcing, remarkably influencing the development of the Asian monsoon, which, in turn, affects large-scale floods and droughts in China. It is thought that a positive snow anomaly on the plateau was one of the prime factors contributing to the 1998 severe floods in the Yangtze River basin and northeastern China (NCC of China, 1999; Reference ChenChen, 2001).

Present-day measurements of temperature profiles in terrestrial boreholes have been used extensively to reconstruct the history of the ground surface temperature (GST) over a large range of spatial and temporal scales (Reference Pollack and SmerdonPollack and Smerdon, 2004). The borehole-based reconstructions of GST have been widely used as indicators of paleoclimate (Reference SmerdonSmerdon and others, 2004). These reconstructions assume that heat transport within the subsurface is purely conductive. Climatic interpretations of GST reconstructions also assume that GST is strongly coupled to surface air temperature (SAT) on timescales of decades and longer (Reference Gosnold, Todhunter and SchmidtGosnold and others, 1997; Reference SmerdonSmerdon and others, 2004). Reference Pollack, Smerdon and van KekenPollack and others (2005) have described a simple representation of this coupling in terms of variable thermal diffusivity in the upper meter of the subsurface. The variability was tied to daily SAT, precipitation and snow cover, but does not incorporate the physical details of these and the many other factors that influence the air–ground interface in many high-fidelity land surface models. Their simple model reduced the difference between observed and modeled temperatures by a factor of 3–4 over a model with uniform diffusivity driven only by SAT. Ground temperatures are generally warmer than air temperatures due to solar radiation effects in the summer and the insulating effect of snow cover during the winter. The low thermal diffusivity of snow dampens surface temperature variations; snow effectively insulates the ground during the coldest part of the year. A numerical model of snow–ground thermal interactions was developed by Reference Bartlett, Chapman and HarrisBartlett and others (2004) to investigate the effect of seasonal snow cover on annual ground temperatures. The model was parameterized in terms of three snow-event parameters: onset time of the annual snow event, duration of the event, and depth of snow during the event. The model was validated using SAT, subsurface temperature at 10cm depth and snow-depth data from the 6 years of observations at Emigrant Pass climate observatory, northwestern Utah, USA, and 217 station years of US National Weather Service data from sites across North America. The measured subsurface temperature–time series was compared to changes predicted by the model. The model consistently predicted ground temperature changes that compared well with those observed. Sensitivity analysis of the model leads to a non-linear relationship between the three snow-event parameters (onset, duration and depth of the annual snow event) and the effect of snow on mean annual GST.

Beginning in 1996, a joint Chinese/Japanese GEWEX (Global Energy and Water Cycle Experiment) Asian Monsoon Experiment (GAME)-Tibet project has been carried out to investigate the effect of the Tibetan Plateau on the Asian monsoon system, to examine the interaction between land and atmosphere processes, and to improve the land surface parameterization scheme in climate models. The preliminary observation experiment was conducted from July to September 1997. During this period, the soil moisture and soil temperature measurement systems (SMTMS) and automatic weather stations were installed at several sites on the northern part of the Tibetan Plateau. The intensive observation period of the GAME-Tibet project was conducted from May to September 1998.

In winter 1997/98, very heavy snowfall occurred on the Qinghai–Xizang (Tibetan) Plateau (Reference ChenChen, 2001), especially in the Amdo–Nagqu region, resulting in the death of a large number of sheep and yaks due to starvation and low temperatures, putting enormous economic stress on local residents. Several GAME-Tibet observation sites are located within the heavy snowfall area. In this paper, we examine the effect of heavy snowfall on ground temperature variations using ground temperature data at different GAME-Tibet observation sites and analyze spatial and temporal variations of ground temperature during 1997/98.

2. Observation Sites and Data Collection

2.1. Observation sites

The observation sites are located predominantly along the Qinghai–Tibet highway (Fig. 1). The site-specific geographic coordinates and elevations are listed in Table 1. Except for the northernmost site (D66), observations were conducted on grazing lands. To prevent damage by animals, the observation sites were enclosed by chain-linked fences. The height of vegetation generally does not vary from site to site, but vegetation density decreases northward.

Fig. 1.

Locations of the observation sites. (σ) Map of the Qinghai–Xizang (Tibetan) Plateau with 3 km contour shown. The study area is outlined. (b) Enlarged maps of the study area. The right frame corresponds to the small square in the left frame. The solid lines represent roads and the filled circles represent observation sites.

Table 1.

Location of observation sites

3. Analysis and Results

The ground temperature (GT) variation decreases with depth, especially for the daily range. Thus, we focus the discussion mainly on the temporal and spatial variation of the daily maximum, the daily minimum and the daily range in the shallowest layer (4cm depth).

3.1. Variation of the daily maximum and minimum ground temperature at different sites

The variations of the daily maximum and minimum GT at 4cm depth (site D105 is 5 cm in depth) at different sites are shown in Figure 2. At site D66, the variation trends are consistent. The daily maximum GT fluctuates more than the daily minimum GT during summer, but the difference is not very marked. The temperature decrease during the period September–January is fundamentally consistent with the temperature increase during the period January–June. At the Tuotuohe site, variations of the daily maximum and minimum GT during winter are also consistent. However, for the whole-year period, the variations are well approximated by sine curves ( Fig. 2 ). This indicates that although stochastic weather processes could affect the GT, its variations are mainly controlled by the solar radiation with a 1 year cycle.

Fig. 2.

The daily maximum and minimum ground temperature at 4cm depth at different sites, 1 August 1997 to 1 October 1998. The solid line is daily maximum temperature and the dotted line is daily minimum temperature. Dates are yy-mm-dd.

For the D105 site, both the temperature decrease in early October and the increase in late April occur more quickly for daily maximum temperature than for daily minimum. In winter, especially from mid-October to mid-February, the maximum and minimum temperatures have approximately the same variation trends. From mid-February to the end of March, the daily maximum increased earlier than the daily minimum. From early May, the daily maximum GT increased quickly, with fluctuations, while the increase in daily minimum GT was relatively slow. As a result, the daily range of the GT is large during the summer.

At site D110, the GT pattern differs from that at more northerly sites. The variations of the daily maximum and minimum GT are inconsistent throughout the year, and do not correspond to a sine curve. The daily maximum and minimum GT fluctuate more in summer than in winter, and the daily maximum GT fluctuates more than the daily minimum. Especially at the end of September, the daily maximum temperature (DMAT) decreases more quickly than the daily minimum temperature (DMIT). Thus, the daily range of the GT (DRGT) decreases rapidly, after which the decrease of the DMAT and DMIT slows down. At this time the DRGT is already quite small. In early May, the DMAT increases rapidly, but the DMIT increases relatively slowly, so the DRGT increases again.

At sites WADD and Amdo, the variations of DMAT and DMIT are almost the same as at D110, but the variation trends of DMAT and DMIT at sites NODA and MS3637 are similar to those at site D105. The variations at site MS3608 are similar to those at Tuotuohe.

3.2. Variation of the daily range of the ground temperature at different sites

To examine the difference in temporal variation between DMAT and DMIT, the DRGT at 4cm depth at different sites was calculated and is presented in Figure 3. The DRGT shows significant temporal and spatial variations. At site D66, it is larger, but fluctuates more, in summer than in winter. At Tuotuohe, the DRGT decreased from the end of August to the end of October, but increased throughout November, except for a sharp decrease around 26 November. It decreased again at the end of March and increased relatively quickly in mid-April. This demonstrates that the variation of the DRGT at Tuotuohe was less regular than at D66.

Fig. 3.

The daily range of the ground temperature at 4 cm depth at different sites. Dates are yy-mm-dd.

At site D105, the DRGT had already decreased by early October, then began to increase. In early November, it showed a small decrease that lasted for more than 3 months. From the end of February to early April it began increasing. At the end of April it increased quickly again. At site D110, the DRGT increased very rapidly from mid-September, but became very small by the end of September. From the end of December 1997 to mid-April 1998, it was <0.2˚C. It increased quickly after early May. The variation of DRGT at site WADD was similar to that at D110. However, the anomalies of DRGT at sites NODA, Amdo and MS3637 were not as significant as at D110. The DRGT began to increase in mid-March, suddenly decreased in early April, then increased but with variability. The trend in variability of the DRGT at site MS3608 was similar to that at Tuotuohe.

4. Discussion

Our analysis shows that significant differences in temporal and spatial variations of the DMAT, DMIT and DRGT occurred from winter 1997 to early 1998 on the northern part of the Tibetan Plateau, as evident from records obtained at an array of sites located from south of the Kunlun Shan (D66) to south of Nagqu (MS3637). At site D110, the DRGT fluctuated within only 0.2˚C from the end of December 1997 to mid-April 1998, but in the north, at site D66, it fluctuated from 5˚C to ∼20˚C at the same depth and during the same period. At the southernmost site (MS3637), the DRGT fluctuated about 1.0˚C from mid-November to early February. From mid-February to mid-March, it increased, reaching 8.1 ˚C. An important question is why the variations of the DRGT in the Nagqu-Amdo region are different from those at site D66. In other words, why are the temporal and spatial distributions of the DRGT in the northern Tibetan Plateau in winter 1997/98 anomalous?

One first needs to know whether or not the above anomalies are related to the effect of the soil moisture content and freezing-thawing processes on the GT The high soil-moisture content could result in a decrease in the DRGT, especially during the snowmelt period. This is easy to understand given that the heat capacity of water is relatively high, and the temperature decrease at night and increase during the day can be slow. This is especially true during the early winter and early summer when daytime temperature is not so high and night-time temperature not so low. If the water content near the GT measurement probe was quite high, such conditions would strongly affect the DMAT, DMIT and DRGT. We first examined site MS3608, located 50 km south of Nagqu. The DRGT was 1.3˚C and 2˚C on 18 December 1997 and 14 January 1998 respectively, but the corresponding DMATs were –5.4˚C and –6.3˚C. Similar conditions also existed on 28 January 1998, when the DMAT was –2.6˚C and the DRGT reached 7.7˚C. However, the soil near the measurement probe did not thaw during this period. Even though the probe was completely surrounded by ice, its effect on the temperature was the same as when there is no ice. At the same site, when the soil freezes completely, the GT variation cannot be explained by variations in soil properties. This shows that the differences in DRGT can only be explained by weather processes and snow-cover variations. It is evident that weather processes could cause the DRGT to decrease, but they could not keep it very low for several months, and certainly could not cause it to fall below 0.2˚C and then stay at that level for more than 4 months, as was the case at site D110. If the variation of DRGT at site D66 was due to weather processes, the variations of DRGT at D110 and other sites could only be caused by snow cover.

The above anomalous variations of DRGT can only be explained by the influence of the very heavy snowfall that occurred within the Amdo–Nagqu region in winter 1997/98. The snow cover thermally insulated the soil surface and modified the energy balance ( Reference Gosnold, Todhunter and SchmidtGosnold and others, 1997; Reference Sokratov and BarrySokratov and Barry, 2002; Reference Stieglitz, Romanovsky and OsterkampStieglitz and others, 2003; Reference Bartlett, Chapman and HarrisBartlett and others, 2004; Reference SmerdonSmerdon and others, 2004; Reference Pollack, Smerdon and van KekenPollack and others, 2005). On the one hand, when the ground is covered by snow it is decoupled from the air temperature that decreases the GT fluctuations. On the other hand, the heat conductivity of snow is small, making it difficult for solar radiation to pass into the soil during the daytime or to be emitted from the ground surface at night. This also causes GT fluctuation to decrease. Moreover, due to the high albedo of snow, less solar radiation is absorbed by the snow-cover surface than by a bare surface. As a result, a relatively severe snow cover would significantly affect the DRGT. In other words, the variation in the DRGT, to some extent, would record the snow cover on the surface.

At present, there are only a few weather stations on the Tibetan Plateau. Most of them are located in river valleys and are not representative of the environmental conditions. Snow cover in the Northern Hemisphere is monitored mainly by means of satellite remote sensing, but the resolution of remotely sensed data is usually low. The SMTMS installed by GAME-Tibet on the northern Tibetan Plateau can be used to evaluate snow cover during winter 1997/98. Although no empirical snow-depth observations were performed, the variations of the DRGT are considered to provide a qualitative reflection of the severity of the heavy snow at different sites on the northern Tibetan Plateau.