黄土高原半干旱区复杂地形上大气边界层湍流特征
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摘要
正确认识黄土高原半干旱区大气边界层湍流对理解区域地-气相互作用基本过程及其气候反馈机理、提高数值天气预报和大气污染预测准确性、揭示气候变化背景下的区域干旱化特征方面有重要意义。而复杂的下垫面条件制约了人们对该区域湍流特征的认识。
为认识黄土高原复杂地形上大气边界层湍流特征,分析了兰州大学半干旱气候与环境观测站(Semi-Arid Climate and Environment Observatory of Lanzhou University,SACOL)的湍流观测资料。浅层土壤热量存储和垂直平流输送是SACOL夏季地表能量不闭合的最主要原因；其他诸如低层空气存储、光合作用固定等因素占10%左右；传感器间距和采样频率等造成涡动相关系统(EC)对湍流热通量估计偏低。这种偏差一方面说明EC也对CO2通量某种程度上低估,另一方面通过WPL修正传递误差影响CO2通量观测精度。在黄土高原半干旱区,白天,强烈的感热输送造成的密度扰动影响强烈,EC观测的CO2通量误差与感热通量有更强的相关性；夜间,CO2浓度和水汽浓度的谱特征一致。
夜间稳定层结,非平稳运动是超临界理查森数条件下湍流存在的重要原因,导致湍流通量离散性大,偏离平均气流的估计值,湍流表现为强烈的水平速度脉动和相对微弱的垂直速度脉动,呈间歇态。将稳定边界层湍流分为“局地湍流”和“非平稳运动”两种运动形态,尺度分析表明两者的临界尺度在2～4mm。弱稳定情形,局地湍流强度是常值,σ无量纲风速标准差σw/u*、σu/u*和σv/u*分别为1.35、2.54和2.21；微风强稳定情形,非平稳运动在湍流生成和通量输送方面起决定作用。提出一判别非平稳运动的方法,可客观定量分离非平稳运动信号,非平稳运动发生频率随风速U增大而减小,U>3.0m s-1时,非平稳运动消失,非平稳风速在1.0m s-1左右,持续时间不超过20min。不同于平坦均匀站点,在复杂地形上风速是研究非平稳运动应关注的主要因素,依非平稳运动和局地湍流特征,复杂地形上稳定边界层湍流可分为三类：(1)平稳湍流(U>3.0m s-1),相似理论较好成立,Φm,=0.7+1.5ξ；(2)间歇湍流,U在一定范围内(梯度理查森数Ri≤0.3时,1.0～3.0ms-1；Ri>0.3,1.5～3.0ms-1),湍流通量由局地湍流和非平稳运动共同贡献,相似理论能用以描述局地湍流,不能描述非平稳运动；(3)弱风区(Ri≤0.3时,U<1.0ms-1；Ri>0.3,U<1.5m s-1),非平稳运动起决定性作用,相似理论失效。
边界层低空急流发生时,其剪切作用是夜间湍流主要能量来源,此时非平稳被压制,87.3%的观测是Ri<0.25的弱稳定层结,湍流活动强,平稳性好,湍流在上层产生并向下传递,湍动能输送强度约-3×10-3m3s-3；无低空急流时,多是Ri>0.25的强稳定情形,非平稳运动频发,湍流间歇性强。
A basic understanding of the characteristics of turbulence in the boundary layer and the fluxes between the earth's surface and atmosphere in the semiarid region of the Loess Plateau is of significance for understanding of the land-atmosphere interaction processes and their climate feedback mechanism, improving the accuracy of numerical weather and air pollution forecast and other aspects. However, the complex terrain limits the understanding on the turbulence of this region.
To gain an insight into the characteristics of turbulence in the boundary layer over the complex terrain of the Loess Plateau, data from the Semi-Arid Climate and Environment Observatory of Lanzhou University (SACOL) are analyzed. Vertical advection and soil heat storage are main sources of imbalance and contribute nearly80%of the energy residuum; the composite of the minor surface energy balance terms, including air heat storage, vertical movement of moisture in soil and photosynthesis, jointly account for10%of the residuum. The flux attenuation due to spatial separation of sensors and sampling frequency could not be ignored, which alerts us to the possibility that CO2flux may also be underestimated. On the other hand, the losses of turbulent energy fluxes influence CO2flux derived from open-path analyser via application of the WPL algorithm. In the semiarid region of the Loess Plateau, during the daytime, the strong density effect caused by sensible heat results in CO2flux observation precision strongly dependent on the sensible heat flux. While in the nighttime, the behavior of CO2concentration spectrum is consistent with that of water vapor concentration.
Non-stationary motions are the important cause of turbulence, resulting in fluxes being scattered, deviating from that estimated by the mean airflow, accompanied by great fluctuations in horizontal velocity but much smaller fluctuations in vertical velocity, and the turbulence is intermittent. Turbulence in a stable boundary layer can be divided into two different forms of movement,"local turbulence" shear generated with small-scale, and "nonstationary motions" with scales just greater than those of the local turbulence, and the scale analysis shows that the critical scale between the two is2-4min. Under weakly satble condition, the standard deviation of u, v, and w normalized by friction velocity u is2.54,2.21and1.35, respectively. The generation of turbulence by non-stationary motions is a dominant factor in turbulence when winds are weak. A method has been proposed to identify and efficiently isolate nonstationary motions from turbulence series, and then the characteristics of non-stationary motions are examined. Nonstationary motions occur more often with decreasing wind speed, and last from a few to20minutes with the nonstationary velocity around1.0m s-1. Unlike site over homogeneous and flat underlying surface where turbulence nonstationarity is a function of stability, over a complex terrain site such as SACOL, the wind speed is a much more significant factor rather than the stability parameter to determine the occurrence frequency of nonstationary motions. Then turbulence is categorized into three regimes based on the behaviors of nonstationary motions and local turbulence. Regime1considers stationary turbulence with a wind speed greater than3.0m s-1, and the Monin-Obukhov similarity theory (MOST) can be used to calculate the turbulence momentum flux. Regime2examines intermittent turbulence where the MOST is competent to evaluate the local turbulence momentum flux, but not nonstationary motions. Regime3involves wind speed that is less than the threshold value, where nonstationary motions are dominant, local turbulence is independent of the mean flow, and where the MOST may well be invalid.
The presence of low-level jets (LLJs) results in strong turbulence and weak stability with gradient Richardson number (Ri) less than0.25by the strong shear. The turbulence is more active and stationary, transported downward from aloft in the boundary layer, about-3×10-3m3s-3. With the absent of jet activity, synchronous observations show that65.4%are strong stable stratification of Ri＞0.3, and non-stationary motions are more frequent.
为认识黄土高原复杂地形上大气边界层湍流特征,分析了兰州大学半干旱气候与环境观测站(Semi-Arid Climate and Environment Observatory of Lanzhou University,SACOL)的湍流观测资料。浅层土壤热量存储和垂直平流输送是SACOL夏季地表能量不闭合的最主要原因；其他诸如低层空气存储、光合作用固定等因素占10%左右；传感器间距和采样频率等造成涡动相关系统(EC)对湍流热通量估计偏低。这种偏差一方面说明EC也对CO2通量某种程度上低估,另一方面通过WPL修正传递误差影响CO2通量观测精度。在黄土高原半干旱区,白天,强烈的感热输送造成的密度扰动影响强烈,EC观测的CO2通量误差与感热通量有更强的相关性；夜间,CO2浓度和水汽浓度的谱特征一致。
夜间稳定层结,非平稳运动是超临界理查森数条件下湍流存在的重要原因,导致湍流通量离散性大,偏离平均气流的估计值,湍流表现为强烈的水平速度脉动和相对微弱的垂直速度脉动,呈间歇态。将稳定边界层湍流分为“局地湍流”和“非平稳运动”两种运动形态,尺度分析表明两者的临界尺度在2～4mm。弱稳定情形,局地湍流强度是常值,σ无量纲风速标准差σw/u*、σu/u*和σv/u*分别为1.35、2.54和2.21；微风强稳定情形,非平稳运动在湍流生成和通量输送方面起决定作用。提出一判别非平稳运动的方法,可客观定量分离非平稳运动信号,非平稳运动发生频率随风速U增大而减小,U>3.0m s-1时,非平稳运动消失,非平稳风速在1.0m s-1左右,持续时间不超过20min。不同于平坦均匀站点,在复杂地形上风速是研究非平稳运动应关注的主要因素,依非平稳运动和局地湍流特征,复杂地形上稳定边界层湍流可分为三类：(1)平稳湍流(U>3.0m s-1),相似理论较好成立,Φm,=0.7+1.5ξ；(2)间歇湍流,U在一定范围内(梯度理查森数Ri≤0.3时,1.0～3.0ms-1；Ri>0.3,1.5～3.0ms-1),湍流通量由局地湍流和非平稳运动共同贡献,相似理论能用以描述局地湍流,不能描述非平稳运动；(3)弱风区(Ri≤0.3时,U<1.0ms-1；Ri>0.3,U<1.5m s-1),非平稳运动起决定性作用,相似理论失效。
边界层低空急流发生时,其剪切作用是夜间湍流主要能量来源,此时非平稳被压制,87.3%的观测是Ri<0.25的弱稳定层结,湍流活动强,平稳性好,湍流在上层产生并向下传递,湍动能输送强度约-3×10-3m3s-3；无低空急流时,多是Ri>0.25的强稳定情形,非平稳运动频发,湍流间歇性强。
A basic understanding of the characteristics of turbulence in the boundary layer and the fluxes between the earth's surface and atmosphere in the semiarid region of the Loess Plateau is of significance for understanding of the land-atmosphere interaction processes and their climate feedback mechanism, improving the accuracy of numerical weather and air pollution forecast and other aspects. However, the complex terrain limits the understanding on the turbulence of this region.
To gain an insight into the characteristics of turbulence in the boundary layer over the complex terrain of the Loess Plateau, data from the Semi-Arid Climate and Environment Observatory of Lanzhou University (SACOL) are analyzed. Vertical advection and soil heat storage are main sources of imbalance and contribute nearly80%of the energy residuum; the composite of the minor surface energy balance terms, including air heat storage, vertical movement of moisture in soil and photosynthesis, jointly account for10%of the residuum. The flux attenuation due to spatial separation of sensors and sampling frequency could not be ignored, which alerts us to the possibility that CO2flux may also be underestimated. On the other hand, the losses of turbulent energy fluxes influence CO2flux derived from open-path analyser via application of the WPL algorithm. In the semiarid region of the Loess Plateau, during the daytime, the strong density effect caused by sensible heat results in CO2flux observation precision strongly dependent on the sensible heat flux. While in the nighttime, the behavior of CO2concentration spectrum is consistent with that of water vapor concentration.
Non-stationary motions are the important cause of turbulence, resulting in fluxes being scattered, deviating from that estimated by the mean airflow, accompanied by great fluctuations in horizontal velocity but much smaller fluctuations in vertical velocity, and the turbulence is intermittent. Turbulence in a stable boundary layer can be divided into two different forms of movement,"local turbulence" shear generated with small-scale, and "nonstationary motions" with scales just greater than those of the local turbulence, and the scale analysis shows that the critical scale between the two is2-4min. Under weakly satble condition, the standard deviation of u, v, and w normalized by friction velocity u is2.54,2.21and1.35, respectively. The generation of turbulence by non-stationary motions is a dominant factor in turbulence when winds are weak. A method has been proposed to identify and efficiently isolate nonstationary motions from turbulence series, and then the characteristics of non-stationary motions are examined. Nonstationary motions occur more often with decreasing wind speed, and last from a few to20minutes with the nonstationary velocity around1.0m s-1. Unlike site over homogeneous and flat underlying surface where turbulence nonstationarity is a function of stability, over a complex terrain site such as SACOL, the wind speed is a much more significant factor rather than the stability parameter to determine the occurrence frequency of nonstationary motions. Then turbulence is categorized into three regimes based on the behaviors of nonstationary motions and local turbulence. Regime1considers stationary turbulence with a wind speed greater than3.0m s-1, and the Monin-Obukhov similarity theory (MOST) can be used to calculate the turbulence momentum flux. Regime2examines intermittent turbulence where the MOST is competent to evaluate the local turbulence momentum flux, but not nonstationary motions. Regime3involves wind speed that is less than the threshold value, where nonstationary motions are dominant, local turbulence is independent of the mean flow, and where the MOST may well be invalid.
The presence of low-level jets (LLJs) results in strong turbulence and weak stability with gradient Richardson number (Ri) less than0.25by the strong shear. The turbulence is more active and stationary, transported downward from aloft in the boundary layer, about-3×10-3m3s-3. With the absent of jet activity, synchronous observations show that65.4%are strong stable stratification of Ri＞0.3, and non-stationary motions are more frequent.
引文
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