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--> --> -->(Eigenmann et al., 2009) investigated near-ground FCCs in the Kinzig Valley, Black Forest, Southeast Germany by using eddy covariance (EC) measurements combined with a Doppler radar system and discussed the applicability of using the EC method to detect FCCs. Following this study, (Zhou et al., 2011) analyzed FCCs in a typical land-lake breeze circulation at Nam Co Station, which is near Nam Co Lake in Tibet. Buoyant forces generated by elevated heating of a mountain slope can induce local mesoscale circulations, usually referred to as upslope winds or anabatic winds (Lee and Kimura, 2001). However, if the land-use type of the highland is forest and the lower land is grass or cropland, it can induce a circulation that is counter to upslope winds (Hanesiak et al., 2004). For this reason, we chose the Qomolangma Monitoring and Research Station for Atmosphere and Environment (QOMS), which has bare soil underlying the surface of a mountain, and the Southeast Tibet Monitoring and Research Station for Environment (SETS), which has forest on a mountain and high grass in a valley, to detect the FCCs and compare the differences. Subsequently, we investigated the influence of the monsoon on FCCs.
QOMS and SETS have similar terrain features but completely different characteristics of underlying surface in the adjacent area. There are probably essential distinctions between the generation mechanism and structure of local small-scale circulation at these two stations. This analysis focuses on discussing the differences in FCCs between the two stations under the influence of specific background circulation and is a supplement to the results of (Eigenmann et al., 2009) and (Zhou et al., 2011). The present study aims to investigate the near-ground FCCs based on EC data at QOMS and SETS, and aims to serve as a reference for further research on local circulation systems.
Figure1. Topographic features (left) and land-use type (right) of (a, b) QOMS and (c, d) SETS. The locations of the two stations are marked by a red cross in each plot.
Figure2. Sensible heat flux (H; units: W m-2), latent heat flux (LE; units: W m-2) and wind direction in 2011 at (a, c, e) QOMS and (b, d, f) SETS.The data used in this study are obtained from the EC tower. An EC system (measurement height: 3.25 m (QOMS) and 3.04 m (SETS); sampling frequency: 10 Hz), equipped with a sonic anemometer (CSAT3, Campbell Scientific Inc., Logan, USA., was used for collecting wind vector and sonic temperature data. An open-path H2O/CO2 gas analyzer (Li-7500, LI-COR Biosciences, Nebraska USA) was used for water vapor and CO2 concentrations observation.
Footprint analyses have to be performed to evaluate the spatial representativeness of measurements. For the present study, a forward Lagrangian footprint model (Rannik et al., 2003) combined with the flux data quality assessment scheme of (Foken and Wichura, 1996) was applied to provide a basis for data filtering (G?ckede et al., 2004, 2006; Eigenmann et al., 2009). Furthermore, the impact of internal boundary layers caused by the discontinuities of surface properties should be checked. The relation proposed by (Raabe, 1983) is as follows: \begin{equation} z\leqslant\delta=0.3\sqrt{x} .\ \ (1) \end{equation} This relation can be used to approximately determine the height δ of the new equilibrium layer (Foken, 2008a) in order to check the impact of the internal boundary (Eigenmann et al., 2009). Here, x is the fetch (m), and z is the height (m) of the sensor. In this study, the effect of the fence is considered as an obstacle. The measuring height of both sites is greater than twice that of the fence height; hence, the influence of the fence on flux measurements can be neglected. Table 1 shows the results for the approximately calculated fetch of the target underlying surface type for QOMS (gravel mixed with grass) and SETS (high grass). "I" presented in this table indicates that the fetch of the target land-use type is sufficiently large to make the internal boundary layer higher than the measurement height. At QOMS, the new equilibrium layer is below the measurement level in the 270° and 300° directions. The flux measurements within these two sectors are under the influence of the internal boundary layer and should be discarded. However, the influence of the heterogeneous underlying surface on the overall assessment was weak because these regions do not lie in the prevailing wind direction. For the case at SETS, the terrain is more complicated and the fetch of the 30°, 60°, 90°, 120°, 330° and 360° sectors denotes the distance between the EC tower and the outer edge of the surface discontinuity. Flux measurements for wind directions of 90° and 120°, where the measuring height of 3.04 m is greater than δ, and 150°, 240°, 270° and 300°, where the measuring height is lower than δ, can be associated with the target land-use type (high grass). The footprint analysis results are also presented in Table 1. Generally, if the flux contribution from the target land-use type was less than 80% and the δ was greater than the measurement height, the flux data should be excluded from further analyses (Mauder et al., 2006).
4.1. Detection of FCCs
The stability parameter ζ, \begin{equation} \zeta=\dfrac{z}{L}=\dfrac{zkg(\overline{w'\theta'_v})_0}{\bar{\theta}_vu_*^3} , \ \ (2)\end{equation} can be used to detect the occurrence of FCCs (Eigenmann et al., 2009). Here, z, L, k, g, w, θv and u* represent measurement height, Obukhov length, von-Kàrmàn's constant, gravitational acceleration, vertical wind speed, virtual potential temperature and friction velocity, respectively. The subscript "0" of \((\overline{w'\theta'_v})_0\) indicates the turbulent flux equal its respective surface value, and \(\overline{w'\theta'_v}\) is the covariance of w and θv. This parameter can be considered as B/S, where \begin{equation} B=\dfrac{g}{\bar{\theta}_v}(\overline{w'\theta'_v})_0 ,\ \ (3) \end{equation} and \begin{equation} S=u_*^2\dfrac{u_*}{kz}=-\overline{w'u'}\dfrac{\partial\bar{u}}{\partial z} .\ \ (4) \end{equation} These are the buoyancy term (B) and the shear term (S) in the TKE function respectively. Free convection occurs when ζ<-1 (Foken, 2008b), i.e., the thermal effect dominates the dynamic effect. In other words, if high buoyancy fluxes coincide with low u*, FCCs will be triggered. To obtain more detailed information on the temporal structure of FCCs, both 30 min and 5 min were used as the average block length of the EC flux data calculation in the present study. Moreover, only flux data with quality flags not exceeding 3 within the 30 min data evaluated by the scheme of (Foken and Wichura, 1996), with the contribution of the target underlying surface exceeding 80% and without disturbance engendered by an internal boundary layer, were used to detect FCCs. In addition, to avoid calculation illusion, the detection of FCCs discarded the data with a sensible heat flux less than 20 W m2.
Figure3. Daily variation of (a1, a2) stability parameters, (b1, b2) sensible and latent heat flux (units: W m-2), (c1, c2) friction velocity and horizontal wind speed (units: m s-1), (d1, d2) downward shortwave radiation (units: W m-2), (e1, e2) wind direction, and (f1, f2) data quality flags of sensible heat flux, (a1-f1) on 12 April 2011 at QOMS, and (a2-f2) on 3 April 2011 at SETS (a2-f2). The vertical gray dotted lines mark the occurrence of FCCs.QOMS is on the northern side of Mt. Qomolangma under the influence of katabatic flow over glaciers (Sun et al., 2007). The influence of downslope katabatic glacier winds (southerly or south-southeasterly) on up-valley winds (north-northeasterly) forced by solar heating delays the onset and weakens the intensity of up-valley winds. Figures 3a1-f1 show a typical day of FCC occurrence on 12 April 2011 at QOMS. In the morning, the glacier wind intensity is not sufficiently strong, and thus thermally driven up-valley winds can occur approximately two hours after sunrise. During the onset of up-valley winds, an increasing sensible heat flux (Fig. 3b1) caused by solar heating occurs with a lower wind speed and u*. The first occurrence of FCCs occurred at approximately 1040 LST and was the result of a horizontal wind speed decrease caused by a change in local circulation from prevailing katabatic glacier winds to prevailing up-valley winds, which was accompanied by increasing buoyancy fluxes. A sudden change in wind direction and an increase in wind speed after 1040 LST (see Figs. 3c1 and e1) implies the domination of thermally induced valley circulation over katabatic glacier winds from 1040 to 1330 LST. After this period, a slightly weak decreasing trend in solar heating (see Fig. 3d1), caused by occasional cloud cover, weakened the intensity of up-valley winds. Meanwhile, the increasing temperature difference between the ice surface and the air nearby strengthens the glacier winds (Sun et al., 2007). Although the transient cloud cover reduces solar heating, the considerable surface heating does not disappear but, rather, is partially weakened. Therefore, during the period from 1330 to 1500 LST, the oscillation of wind direction caused by local circulation variation induces the occurrence of a low wind speed together with high buoyancy, i.e., the occurrence of FCCs. However, during the monsoon, the circumstance is different and will be discussed in section 4.3.
Figures 3a2-f2 show a classic case of the occurrence of FCCs on 3 April 2011 at SETS. Figures 4c2 and 4e2 show that down-valley winds become inconspicuous during the night and u* maintains a lower value before sunrise. Unlike at QOMS, FCCs do not just occur during lower wind-speed periods. Therefore, the occurrence of FCCs (approximately from 0940 to 1200 LST) is not the result of a decrease in horizontal wind speed but is triggered completely by strong solar heating. Shortly after 1200 LST, the persistent enhancement of upslope wind speeds led to the buoyancy term not being able to dominate the shear term any longer, resulting in the disappearance of FCCs.
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4.2. Near-ground boundary layer structure during FCCs
The continuous wavelet transform (CWT) is used to analyze the turbulent spectra. This spectral operator was applied to analyze the turbulent structure of vertical wind speeds and temperatures during the period from 0900 to 1700 LST (480 min) at QOMS and from 0800 to 1600 at SETS using the same data analyzed in Fig. 3. The CWT was completed using SOWAS——the Software for Wavelet Spectral Analysis and Synthesis (Maraun and Kurths, 2004; Maraun et al., 2007). To eliminate the effect of diurnal variation and reduce the processing time, the raw data were detrended and block averaged from the original 10 Hz to 0.5 Hz before the CWT calculation.Figures 4a and b show the normalized wavelet power spectra of the vertical wind speed and air temperature at QOMS, respectively. It is significant that lower-frequency turbulence contributes more spectral power during the first FCC period, marked by the black dotted vertical lines. The time scale of air in plumes or thermals cycling once between the bottom and the top of the mixed layer is approximately 5 to 15 min in a well-developed convective boundary layer (Stull, 1988). The structure of large-scale turbulence (lower-frequency turbulence) presented in Fig. 4a conforms to this thermal characteristic. The white dotted vertical lines mark the start and end time of the second FCC period, during which large-scale turbulence still contributes more power but it is not as obvious as during the first FCC period. This dynamic may be the result of higher wind speeds during the second period.
Figure4. CWT analysis of the (a, c) vertical wind speed and (b, d) air temperature, (a, b) from 0900 to 1700 LST (480 min) on 12 April 2011 at QOMS, and (c, d) from 0800 to 1600 LST (480 min) on 3 April 2011 at SETS. Two black dotted lines marked the period of FCCs during morning and the yellow dotted lines marked the period of FCCs during afternoon.The situation at SETS, as depicted in Figs. 4c and d, is different from that at QOMS. The period marked by the black dotted vertical lines contains a low wind-speed period before sunrise and the onset of FCCs. At the onset of FCCs, the spectral power is contributed mostly by large-scale turbulence. Moreover, this circumstance does not just occur during FCCs, and there is even larger-scale turbulence outside FCC periods. A possible interpretation is that the considerable heterogeneity of the land surface and the resulting internal boundary layers at SETS (see Fig. 1d) induce low-frequency turbulence.
It is worth noting that the scale of some turbulence is greater than 30 min, which means the EC calculation method cannot capture all types of turbulence power. The average near-ground energy balance closure at QOMS and SETS is 74% and 72%, respectively. Turbulence with scales greater than 30 min led to the imbalance of surface energy.
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4.3. Distribution of FCCs during the entire year
Because both QOMS and SETS are in a region under a monsoonal influence, the existence of differences between the monsoon and non-monsoon seasons should be considered. Figure 5a shows the distribution of FCCs during 2011, excluding the period when precipitation and sensible heat fluxes were less than 20 W m-2. The onset of FCCs is most common from 1.5 to 2 h after sunrise during non-monsoon periods and approximately 4 h or more after sunrise during the monsoon season. To obtain accurate FCC distribution characteristics during the monsoon without confusion caused by data blackout during September and October, supplementary analysis based on a 30 min block average was performed with a more complete data record from 2014. The results indicate that the occurrence of FCCs during the monsoon become more dispersed and less frequent than during the non-monsoon season.During the monsoon season, katabatic glacier winds (southerly or south-southeasterly) cease during the night (see Fig. 2e). This disappearance allows the horizontal wind speed decrease caused by the wind-direction change from katabatic glacier winds to up-valley winds in the morning to cease, undermining the onset of FCCs. Moreover, because of increased water vapor content during the monsoon season, the sensible heat flux is not very high——normally less than 200 W m-2. FCCs can only occur with a lower wind speed in most cases. A few hours after sunrise, the temperature difference between the ice surface and air nearby strengthened by solar heating leads to the onset of down-valley glacier winds (Sun et al., 2007). In other words, both up-valley winds and down-valley glacier winds are induced by solar heating. Thus, when the intensity of solar heating is close to an appropriate range, the horizontal wind direction is likely to oscillate between two directions. This oscillation leads to the horizontal wind speed decreasing, and then, FCCs to occur. Take 22 July 2011 as an example (figures not shown). During FCC periods, the range of sensible heat flux is approximately 50-200 W m-2, and the wind speed decreases because of the oscillation of the wind direction from 0° to 45°.
At SETS, the situation is much simpler, because the trigger mechanism of FCCs is no longer the low horizontal wind speed coupled with higher sensible heat flux, but strong solar heating, independently. Figure 5c shows the distribution of FCCs at SETS in 2011. The occurrence of FCCs is approximately one hour after sunrise, and there is no obvious difference between the monsoon and non-monsoon periods, except for the increasing probability of FCC occurrence caused by more frequent cloud cover during the afternoon during the monsoon.
Figure5. Distribution of FCCs in (a) 2011 and (b) 2014 at QOMS and (c) at SETS in 2011. The dashed lines indicate sunrise and sunset, and the gray vertical dotted lines outline the monsoon season.