‘Surface Drag in the Arctic Marginal Sea-ice Zone: A Comparison of Different Parameterisation Concepts’

Two parameterisation schemes for the turbulent surface fluxes and drag coefficients over the Arctic marginal sea-ice zone (MIZ) are (further) developed, and their results are compared with each other. Although the schemes are based on different principles (flux averaging and parameter averaging), the resulting drag coefficients differ only slightly in the case of neutral and stable stratification. For unstable stratification and sea-ice conditions being typical for the north-eastern Fram Strait, the drag coefficients resulting from the parameter-averaging concept are 5–10% larger than those of the flux-averaging concept. At a sea-ice concentration of 45%, the parameter-averaging method overestimates the heat fluxes by a factor of 1.2. An inclusion in the schemes of form drag caused by floe edges and ridges has a much larger effect on the drag coefficient, and on the momentum fluxes, than the choice between the parameter-averaging or flux-averaging methods. Based on sensitivity studies with the flux-averaging scheme, a simple formula for the effective drag coefficient above the Arctic MIZ is derived. It reduces the computational costs of the more complex parameterisations and could also be used in larger scale models. With this simple formula, the effective drag coefficient can be calculated as a function of the sea-ice concentration and skin drag coefficients for water and ice floes. The results obtained with this parameterisation differ only slightly from those using the more complex schemes. Finally, it is shown that in the MIZ, drag coefficients for sea-ice models may differ significantly from the effective drag coefficients used in atmospheric models.     

Summer boundary-layer height at the plateau site of Dome’C,antarctica

Measurements of the mean and turbulent structure of the planetary boundary layer using a sodar and a sonic anemometer, and radiative measurements using a radiometer, were carried out in the summer of 1999–2000 at the Antarctic plateau station of Dome C during a two-month period. At Dome C strong ground-based inversions dominate for most of the year. However, in spite of the low surface temperatures (between −50 and −20 °C), and the surface always covered by snow and ice, a regular daytime boundary-layer evolution, similar to that observed at mid-latitudes, was observed during summertime. The mixed-layer height generally reaches 200–300 m at 1300–1400 LST in high summer (late December, early January); late in the summer (end of January to February), as the solar elevation decreases, it reduces to 100–200 m. A comparison between the mixed-layer height estimated from sodar measurements and that calculated using a mixed-layer growth model shows a rather satisfactory agreement if we assign a value of 0.01–0.02 m s⁻¹ to the subsidence velocity at the top of the mixed layer, and a value of 0.003–0.004 K m⁻¹ to the potential temperature gradient above the mixed layer.     

The Neutral, Barotropic Planetary Boundary Layer, Capped by a Low-Level Inversion

The presence of a low-level, capping inversion layer will affect the height and structure of the planetary boundary layer (PBL). Results from models of varying levels of sophistication, including analytical, turbulent kinetic energy (TKE), second-order closure (SOC), large-eddy simulation (LES) and direct numerical simulation (DNS) models, are used to investigate this influence for the neutral, barotropic PBL. Predicted and observed profiles of stress and geostrophic departure components, and integral measures, such as the parameters of Rossby-number similarity theory, are compared for the KONTUR, Marine Stratocumulus, JASIN, Leipzig, Pre-Wangara and Upavon field experiments.Analytical models of the equilibrium value of inversion height z_i, which depend on the surface friction velocity u_*, and both the Coriolis parameter f and the free-flow Brunt-Väisälä frequency N, are found to give reasonable estimates of the PBL height. They also indicate that only the KONTUR and Marine Stratocumulus experiments were strongly influenced by N. More quantitative comparisons would require larger, more comprehensive datasets. The effects of the presence of a capping inversion on the profile structure were found to be insignificant for h_* = |f|z_i/u_* > 0.15.The simple analytical model performed quite well over all values of h_*; it predicted the profiles of the longitudinal stress component (in the direction of the surface stress) better than the lateral component. The more advanced models performed well for small values of h_* (for flow over the sea), but systematically underestimated the cross-isobaric angle for flow over land. These models predicted the profiles of the lateral stress component better than the longitudinal component. The profiles of the analytical model agreed with those of the advanced models when the constant eddy viscosity of the outer layer was increased.Agreement with DNS was achieved by increasing the eddyviscosity of the analytical model by a factor of 5.Zilitinkevich and Esau(2002, Boundary-Layer Meteorology, 104, 371–379)suggest that the neutral, barotropic values of A and B of Rossby-numbersimilarity theory are not universal constants, but depend on the ratio N/|f|. The dependence for A and B is calculated using the analytical model and TKE models. Over the sea (h_* 0.1; N/|f| 100, where we have used the Zilitinkevich-Esau relation to convert between h_* and N/|f|) there is agreement between the model predictions and observations; however over land where the equilibrium boundary-layer height is greater (h_* 0.35; N/|f| 10) the inconsistency between the advanced model predictions (TKE, SOC, LES, and DNS) and observations, as noted previously by Hess and Garratt, still exists. We attribute this disagreement to violations of the strict assumptions of steady, horizontally homogeneous, neutral, barotropic conditions implicit in the observations. At small values of z_i and a strongly stable background stratification (h_* 0.04; N/|f| 1000) both the TKE and analytical models predict that A and B depend significantly on h_*, however observations are unavailable to confirm these predictions. Zilitinkevich and Esau call this case the `long-lived near-neutral PBL', and state that it is found in cold weather at high latitudes.     

采用经典大地测量技术确定珠峰大地高(2005)的研究

以往对常规测量数据进行处理时,常采用平面与高程分别平差得出珠峰峰顶(山头或觇标)相应于某椭球的平面位置(经纬度)与大地高。提出采用平面与高程进行联合处理的方法,并就这两种方法采用的模型、数据处理方法及最终结果(主要是大地高)进行讨论与分析,并与GPS的结果进行比较,分析其差异。     

BPSA混合策略在GPS高程拟合中的应用

针对误差反向传播(BP)算法训练速度慢和易于陷入局部最小值的缺点,利用BP算法监督学习特点,模拟退火算法(SA)在局部极小处的概率突变性,有效结合BP和SA算法,提出一种BPSA混合学习策略。将其应用于GPS高程拟合,并以实例验证了该算法的有效性。     

茂名城区GPS拟合高程精度的探讨

GPS控制网在联测水准点的基础上,利用GPS水准高程来实现GPS网点的大地高向正常高转换,其精度主要受所拟合的似大地水准面、已知点高程和GPS网点大地高3种误差的影响。     

计算转换参数提高手持式GPS接收机定位精度的方法与探讨

通过在矿区施测的静态GPS控制测量,根据实际不同的坐标系工程用图需要,在矿区内均匀选择三个以上公共点的两套坐标,探讨对手持式GPS接收机求取其转换参数的方法,采用五参数转换法,求出转换参数,然后在手持GPS接受机上设置五参数来提高定位精度.     

GPS高程异常拟合精度的探讨

GPS技术在测量领域已广泛应用,但GPS拟合高程精度制约了其在领域内的推广普及。选择不同的高程异常拟合模型,对GPS高程拟合精度非常重要。通过对驿城区城市控制网进行不同数学模型的GPS高程异常拟合,验证了选择合适的拟合模型及分布合理的高精度水准点,能够解算出高精度的GPS拟合高程,满足一般测量工程的需要。     

鲁西南8-9月份阴雨日数与前期大气环流关系

对鲁西南1979-2008年8-9月份阴雨日数进行统计分析,发现8-9月份阴雨日数总体呈上升趋势;与前期北半球500hPa月平均高度场进行相关分析,结果表明：8-9月份阴雨日数与北半球500hPa平均高度场存在显著的滞后相关性,共得出45个优势相关区,相关区具有明显的区域性,大多数优势相关区出现在60篘以南地区。阴雨日数与前期极涡位置及强弱有很好的对应关系。从优势相关区提取的预报因子具有明显的季节性,上一年秋冬季预报因子占6/9;建立预报方程,试用效果较好。