Uncertainties in Quantitatively Estimating the Atmospheric Heat Source over the Tibetan Plateau

ATMOSPHERIC AND OCEANIC SCIENCE LETTERS, 2014, VOL. 7, NO. 1, 28 33 Uncertainties in Quantitatively Estimating the Atmospheric Heat Source over the Tibetan Plateau DUAN An-Min 1, 3, WANG Mei-Rong 1, 2, and XIAO Zhi-Xiang 1, 2 1 State Key Laboratory of Numerical Modeling for Atmospheric Science and Geophysical Fluid Dynamics, Institute of Atmospheric Physics, Chinese Academy of Sciences, Beijing 100029, China 2 University of Chinese Academy of Sciences, Beijing 100049, China 3 Nanjing University of Information Science & Technology, Nanjing 210044, China Received 5 July 2013; revised 2 August 2013; accepted 19 August 2013; published 16 January 2014 Abstract As a huge, intense, and elevated atmospheric heat source (AHS) approaching the mid-troposphere in spring and summer, the Tibetan Plateau (TP) thermal forcing is perceived as an important factor contributing to the formation and variation of the Asian summer monsoon. Despite numerous studies devoted to determine the strength and change of the thermal forcing of the TP on the basis of various data sources and methods, uncertainties remain in quantitative estimation of the AHS and will persist for the following reasons: (1) Routine meteorological stations cover only limited regions and show remarkable spatial inhomogeneity with most distributed in the central and eastern plateau. Moreover, all of these stations are situated at an altitude below 5000 m. Thus, the large area above that elevation is not included in the data. (2) Direct observations on heat fluxes do not exist at most stations, and the sensible heat flux (SHF) is calculated by the bulk formula, in which the drag coefficient for heat is often treated as an empirical constant without considering atmospheric stability and thermal roughness length. (3) Radiation flux derived by satellite remote sensing shows a large discrepancy in the algorithm in data inversion and complex terrain. (4) In reanalysis data, besides the rare observational records employed for data assimilation, model bias in physical processes induces visible errors in producing the diabatic heating fields. Keywords: Tibetan Plateau, atmospheric heat source, data bias, uncertainties Citation: Duan, A.-M., M. R., Wang, and Z.-X. Xiao, 2014: Uncertainties in quantitatively estimating the atmospheric heat source over the Tibetan Plateau, Atmos. Oceanic Sci. Lett., 7, 28 33, doi:10.3878/j.issn.1674-2834.13.0064. 1 Introduction The Tibetan Plateau (TP), located in the subtropical central and eastern Eurasian continent, acts as a huge, elevated atmospheric heat source (AHS) in spring and summer (Flohn, 1957; Ye and Gao, 1979, Wu et al., 2012). Results based on both data analysis and numerical simulation have revealed that the thermal forcing of the TP facilitates an early monsoon onset with strong East Asian summer monsoon circulation to its east and a dry and hot climate in mid-asia to its west (Duan and Wu, Corresponding author: DUAN An-Min, amduan@lasg.iap.ac.cn 2005; Duan et al., 2013). In interannual variability, strong diabatic heating over the TP generally leads to abovenormal precipitation in the Yangtze and Huaihe River basins (Zhao and Chen, 2001; Duan and Wu, 2004; Wang et al., 2013). During recent years, increasing attention has been paid to the decadal change or long-term trend in AHS over the TP and its possible impact on the Asian summer monsoon and climate change in the surrounding areas (Zhu et al., 2007; Liu et al., 2012; Duan et al., 2013). Results suggest that the overall southward retreat of the rainfall belt of the East Asia summer monsoon is closely related to the weakened AHS over the plateau. Due to rare observational records and inhomogeneous distribution of meteorological stations, many previous studies have estimated the intensity and trend in AHS over the plateau by using reanalysis data. By the adopting reverse computation method, for example, Zhu et al. (2007) calculated the trend in AHS over the TP by using National Centers for Environmental Prediction/National Center for Atmospheric Research (NCEP/NCAR) reanalysis from 1960 to 2004. Their results show that the AHS over the TP underwent a persistent downward trend in spring and summer, particularly during the most recent 20 years. However, results from different reanalysis datasets are not completely consistent, with some even showing opposite signals. Wang et al. (2012) compared the trends of AHS over the TP during 1980 2008 in three reanalysis datasets. They identified decreasing trends in NCEP/NCAR and NCEP/Department of Energy (DOE) and an increasing trend in Japanese 25-year Reanalysis (JRA-25). On the basis of station observations and satellite data from the International Satellite Cloud Climatology Project (ISCCP), Duan and Wu (2008) revealed a persistent weakening trend in AHS, particularly in the spring sensible heat flux (SHF) over the TP since 1980s. Yang et al. (2011a, b) argued that the effect of the heat exchange and biases of the surface net radiation in satellite data and in the China Meteorological Administration (CMA) gaugemeasured precipitation loss may influence the trend in AHS. Their result of the trend in AHS over the entire TP during 1984 2006 was 7 W m 2 per decade, which is much weaker than that reported by Duan and Wu (2008) at 12 W m 2 per decade during 1984 2003. Therefore, uncertainties are apparent in the accurate estimation of the AHS over the TP. The aim of the study is to provide a

NO. 1 DUAN ET AL.: ATMOSPHERIC HEAT SOURCE OVER THE TIBETAN PLATEAU 29 comprehensive discussion on this topic by comparing the results from a variety of data sources and methods. 2 Data and methods The data used in this study include the following sources: 1) Regular surface meteorological observations with an initial quality control provided by CMA. Data were gathered four times daily at 2:00, 8:00, 14:00, and 20:00 Beijing time (BJT). Variables include surface air temperature (T a ), ground surface temperature (T s ), wind speed at 10 m above the surface (V), and daily accumulated precipitation (P r ). 2) ISCCP (http://isccp.giss.nasa.gov/projects/flux.html) and the Global Energy and Water Cycle Experiment- Surface Radiation Budget (GEWEX-SRB, http://eosweb. larc.nasa.gov/prodocs/srb/table_srb.html) satellite radiation data. Radiation fluxes include downward and upward shortwave and longwave fluxes at the top of the atmosphere and at the surface. Both datasets are from 1984 to 2007, with horizontal resolutions of 2.5 2.5 and 1 1. 3) Daily mean diabatic heating data from three reanalysis products of NCEP/DOE (Kanamitsu et al., 2002), JRA-25 (Kazutoshi et al., 2007), and ERA-Interim produced by the European Centre for Medium Range Weather Forecasts (Dee et al., 2011). The horizontal resolution was 1.875 1.88 for NCEP/DOE, 1.125 1.12 for JRA-25, and 1.5 1.5 for ERA-Interim. The numerical prediction models, assimilation programs, and observing systems from NCEP/DOE are nearly the same as those from NCEP/NCAR; some errors in the latter were corrected, and some improvements are primarily reflected in surface temperature, radiation flux, surface water balance, and other surface fluxes. In particular, the rainfall data assimilation significantly improved model simulation of soil moisture (Zhao et al., 2010). Therefore, the NCEP/DOE reanalysis dataset may be considered as an updated version of NCEP/NCAR (Zhao et al., 2010, Zhao and Fu, 2006; Kanamitsu et al., 2002). Because both ISCCP and GEWEX-SRB data are available during 1984 2007, to convenient compare AHS in terms of intensity and trend between station-derived results and reanalysis data, we chose this period for all datasets. Moreover, the most significant trend in AHS over the plateau that occurred in spring (March May) during the last decades (Duan and Wu, 2008; Wang et al., 2012; Zhu et al., 2012), the spring mean AHS, and each component were selected for discussion. For a given region, the AHS (sink) is defined by air column heat gain (loss) and can be expressed as AHS=SHF+LH+RC, (1) where SHF represents the local surface sensible heat transfer, LH is the latent heat released to the atmosphere due to condensation, and RC is the net radiation flux of the air column. For calculation of SHF, the bulk aerodynamic method is widely used: SH C C V ( T T ), (2) p a DH s a where C p =1005 J kg 1 K 1 is the specific heat of dry air at constant pressure, ρ a is air density that decreases exponentially with elevation, and C DH is the (dimensionless) drag coefficient for heat that generally increases with land surface roughness. LH can be roughly calculated by precipitation by LH Pr L w w, (3) where L w = 2.5 10 6 J kg 1 is the condensation heat coefficient, and ρ w denotes water density, and the subscript w refers the water. RC R R ( S S ) ( S S ) 0 0 0 ( F0 F0 ) F, (4) where R and R 0 are the net radiation values at the top of the atmosphere and at the Earth s surface, respectively. S and F denote shortwave and longwave radiation fluxes, respectively; and 0 denote the top of the atmosphere and the ground surface, respectively; and and represent downward and upward transfer, respectively. 3 Results 3.1 Uncertainties in SHF and LH based on station distribution Limited by the remote location, inclement climate, and sparse population, significantly fewer routine meteorological stations are situated over the TP than those in other regions of China. The density of surface meteorological stations within the TP domain is only 34 per million km 2, which is significantly lower than the average of 260 per million km 2 over China. Although researchers investigating the AHS over the TP often adopt records from 73 stations, the spatial distribution is remarkably inhomogeneous. As shown in Fig. 1a, most of the stations are located in the central and eastern TP, east of 85 E, whereas only two are located in the western TP, west of 85 E. Therefore, because the AHS derived by station observations can effectively represent actual conditions only in the central and eastern TP, most of the existing studies based on station observations focus mainly on this area. In addition to the spatial inhomogeneity, altitude positions of meteorological stations may also induce uncertainty in estimating the AHS. Table 1 shows that grids with elevations higher than 5000 m above sea level over and around the TP domain (25 40 N, 75 105 E) account for 31% of the total; those between 4000 m and 5000 m account for 33%; those between 3000 m and 4000 m account for 19%; and those between 2000 m and 3000 m accounts for 17%. However, no stations have elevations above 5000 m. In fact, there are only 17 stations above 4000 m, 29 with elevations between 3000 m and 4000 m, and 27 between 2000 m and 3000 m, accounting for 23%, 40%, and 37%, respectively. Thus, station data can depict the meteorological variables only below 5000 m; records above 5000 m are incomplete for nearly one-third of the TP. We plotted the spring mean and linear trends in T a, T s, V, SHF, and LH during 1984 2007 over the central and eastern TP, which were sorted by elevation, in Figs. 1b e. The climatology characteristics of T a, T s, and LH de-

30 ATMOSPHERIC AND OCEANIC SCIENCE LETTERS VOL. 7 Figure 1 (a) Terrain height (units: m) over and around the Tibetan Plateau (TP) and the locations of 73 meteorological stations across the plateau. Open circles, solid circles, and stars denote the stations with elevations at 2000 3000 m, 3000 4000 m, and 4000 5000 m, respectively. Elevation dependence of (b, c) spring mean and (d, e) linear trend of the T a (units: C and C per decade), T s (units: C and C per decade), V (units: m s 1 and m s 1 per decade), local surface sensible heat transfer (SHF) (units: W m 2 and W m 2 per decade), and latent heat released to the atmosphere due to condensation (LH) (units: W m 2 and W m 2 per decade) during 1984 2007 are averaged by 71 stations over the central and eastern TP. Table 1 Numbers and proportions of routine meteorological stations and grid points at various classifications according to the elevation over the TP. Stations (73) Grids (10859) 2000 height<3000 27 (37%) 1804 (17%) 3000 height<4000 29 (40%) 2082 (19%) 4000 height<5000 17 (23%) 3553 (33%) 5000 height 0 (0%) 3420 (31%) creased with an increase in elevation, whereas the opposite case occurred in V and SHF. For climate change, a robust upward trend occurred in T a and T s at all stations. The warming amplitude in T a presents a clear elevation-dependent feature such that it decreased gradually with elevation ascent. The case for T s differed somewhat; the largest trend appeared within 2000 3000 m but no clear difference was detected at 3000 4000 m and 4000 5000 m. For the annual mean and winter mean in T s, previous studies (Liu and Chen, 2000; Qin et al., 2009) reported a tendency for the warming trend to increase with the elevation in the TP and its surrounding areas. Our results were similar. We detected a warming rate increase from 3000 m to 5000 m above sea level, whereas the warming trend in T s below 2000 m was nearly equal to that above 4000 m. Given the differences in the period, data, and season for research, the results may vary to some degree. The near surface wind speed V decelerated systematically with the largest amplitude appearing within 3000 4000 m and again at 4000 5000 m. The results of the two components of the AHS, i.e., SHF and LH, differed completely, with the former showing a clear weak-

NO. 1 DUAN ET AL.: ATMOSPHERIC HEAT SOURCE OVER THE TIBETAN PLATEAU 31 ening trend and the latter showing an increasing trend. The amplitude in the SHF change is obviously larger than that in LH and was enhanced with height increase; this feature was particularly significant at 4000 5000 m. Considering the fact that no observation exits above 5000 m and the station proportion with elevations between 4000 m and 5000 m is much less than that lower than 4000 m, both the intensity and trend in SHF over the TP might be underestimated by using station observations. Moreover, the region higher than 5000 m above sea level is largely covered by glaciers and snow, which may also cause large uncertainties in evaluating the intensity and trend in the all of the studied parameters. In addition to data coverage, the bulk formula in Eq. (2) includes further bias in calculating SHF because direct SHF observation is absent in most routine stations. A definitive method for determining the C DH value over the TP has not been reported. Ye and Gao (1979) synthesized previous results to give the mean value of C DH as 8 10 3 over the TP. On the basis of data from the Qinghai-Xizang Plateau Meteorological Sciences Experiment (QXPMEX), Chen and Wong (1984) put forward a ten-day averaged C DH parameterized scheme. Afterward, Chen et al. (1985) obtained a smaller value of 4 10 3 by using this parameterized scheme. On the basis of data from two (four) sets of automatic weather stations over the western (central and eastern) TP from July 1993 to March 1999, Li et al. (2000, 2001) estimated the C DH value by using the flux-profile relationship, with results of 6 6.4 10 3 at the western TP and 4.8 10 3 at the central and eastern TP. Recently, Yang et al. (2011b) discussed the differences between methods for estimating the trend in SHF over the TP for the period 1984 2006. Their results indicated that C DH depends on atmospheric stability and thermal roughness length and varies in both temporal and spatial domains. Assuming C DH is a constant value or a simple function of wind speed will induce bias in the trend of SHF, although the climatology is nearly same. Furthermore, real LH intensity obtained by using Eq. (3) with precipitation data may be underestimated systematically at all stations for the precipitation loss in measurement due to wind-induced undercatch, wetting loss, and trace amounts of precipitation (Ye et al., 2004). Wind-induced gauge undercatch was determined to cause the greatest error in most regions, whereas the latter two aspects of are important in low-precipitation regions in northwestern China (Ye et al., 2004). 3.2 Uncertainties in RC induced by satellite data retrieval Because there is a lack of ground-based radiation flux data at the top of atmosphere and the data quality of station-observed surface long wave radiation flux is questionable, one component of the AHS, i.e., RC, is typically derived by satellite remote sensing data. Relative to SHF and LH, the uncertainties of RC in terms of intensity and trend are comparable. To demonstrate this point, we plotted in Fig. 2 the temporal evolution and liner trend in RC in spring during 1984 2007 over the central and eastern TP in both GEWEX-SRB and ISCCP data. RC in GEWEX-SRB was approximately 10 W m 2 less than that in ISCCP in many years. Moreover, the trend between the two shows a large difference in amplitude. The trend in RC during 1984 2007 was 4.9 W m 2 per decade and 2.1 W m 2 per decade in ISCCP and GEWEX-SRB, respectively. As documented by many authors, this discrepancy is induced mainly by the uncertainty in net radiation fluxes at the ground surface because retrieval of the surface radiation budget is more difficult than that at the top of the atmosphere (Yang et al., 2011a; Wang et al., 2012). 3.3 Uncertainties in AHS in reanalysis data Figure 3a shows the spring mean AHS and each component over the central and eastern TP during 1984 2007 determined on the basis of observation and three reanalysis datasets. The average AHS, SHF, LH, and RC from 71 stations was 37 W m 2, 60 W m 2, 29 W m 2, and 52 W m 2, respectively, denoting the dominant contribution of SHF to the overall intensity of AHS before the rainfall season. However, both LH intensity and its contribution in reanalysis data, particularly in ERA-Interim, were larger than those in the station data. In addition, the observed intensity in RC and SHF was stronger in observation than that in all three reanalysis datasets to a different degree. Therefore, the overall intensity of AHS in JRA-25 is nearly twice of observation-based results at 71 stations. Figure 3b shows the linear trend and error estimation in AHS during this period. Relative to climatology, changes in AHS over the TP present a larger discrepancy with a higher uncertainty. The sign in SHF change in all reanalysis datasets corresponded with station-based results; however, similar amplitude was detected in only JRA-25. Generally, no significant trend exited in all terms of diabatic heating and in the total AHS in ERA-Interim. In JRA-25, the large positive trend in LH compensated for the sum of negative trends in SHF and RC and led to an opposite change signal in AHS. In NCEP/DOE, changes in LH and RC were very weak, thereby causing the significant negative trend in SHF to result in a weakened spring AHS. Overall, NCEP/DOE provided the most similar change in AHS to observation-based results over the central and eastern TP but had nearly twice the amplitude. Therefore, uncertainties in trends in diabatic heating are larger than those in climatology over the TP. More Figure 2 Temporal evolutions of spring mean air column net radiation flux (net radiation flux of the air column (RC), units: W m 2 ) over the central and eastern TP (28 38 N, 85 105 E) from datasets of the International Satellite Cloud Climatology Project (ISCCP; black line) and Surface Radiation Budget (SRB; red line) recorded during 1984 2007.

32 ATMOSPHERIC AND OCEANIC SCIENCE LETTERS VOL. 7 Figure 3 (a) Spring mean and (b) linear trend in atmospheric heat source (AHS), LH, RC, and SHF over central and eastern TP during 1984 2007 determined on the basis of observational data and three reanalysis datasets. Units for climate mean and trend are W m 2 and W m 2 per decade, respectively. Bars indicate uncertainty at the 95% confidence level based on standard deviation. All results in reanalysis data have been interpolated onto the locations of 71 stations and ISCCP radiation flux data to estimate RC at the stations. remarkably, uncertainties in observation-based results also exist, particularly for trends in AHS and RC. Hence, adequate observation covering more areas is imperative for obtaining a deeper understanding of the role of thermal forcing of the TP in climate regime and variability. 4 Concluding remarks Diabatic heating fields over the TP show multi-scale variation in both space and time. In this work, we presented a comprehensive discussion on the uncertainties in accurate estimation of the AHS over the TP in terms of intensity and trend. The factors related to these uncertainties arise primarily from the absence of sufficient observational records; imperfect theories, methods, and models further aggravate the situation. Two components of AHS, i.e., SHF and LH, can be calculated directly from historical records at routine meteorological stations. Bias in the former appears to be larger than that in the latter due to the absence of actual SHF observation. Researchers calculating SHF by the bulk formula with T s T a and V generally choose the drag coefficient for heat, C DH, as an empirical constant without considering atmospheric stability and thermal roughness length, which results in further uncertainty, particularly in the trend of SHF. Nevertheless, observation-based results indicate that both intensity and trend in SHF over the TP are enhanced with elevation increase. Because no routine stations exist above 5000 m, the contribution of SHF to the total heat source may be underestimated, according to the existing outcomes based on observation. RC can be determined thus far only by satellite remote sensing data. The uncertainty in RC over the TP is by no means less than SHF or LH due to short length limitations and the evident discrepancy among various data sources induced by algorithms in data inversion and complex terrain. In reanalysis data, rare observational records for data assimilation and model bias in physical processes also induce many errors in producing the diabatic heating fields over the TP. Moreover, further uncertainties in estimating the atmospheric apparent heat source/sink occur in the adoption of the reverse computation method for the error in vertical velocity (Wang et al., 2012) induced by extremely inhomogeneous topography (Yanai and Tomita, 1998; Wang and Zeng, 2012). In the future, it is necessary to established more routine and automatic meteorological stations over the TP, particularly for regions in the northwest and at high elevations. Observation in surface heat fluxes should be included at more stations. In addition, calibration of satellite-derived radiation flux data is essential for obtaining accurate AHS in terms of both intensity and variation. Acknowledgements. We sincerely thank the two anonymous reviews for their helpful comments and suggestions on the manuscript. 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