台湾浅滩浅海水深SAR遥感探测实例研究

本文基于浅海地形SAR遥感成像机理,提出星载SAR图像浅海水深遥感探测新技术.利用该遥感探测新技术与浅海地形SAR遥感图像,在台湾浅滩海域进行了浅海水深SAR遥感探测实例研究.SAR遥感探测水深值与实测水深值的比较结果显示,SAR遥感探测水深值的均方根误差达到2.5 m,误差小于10%.表明SAR具有探测浅海水深的能力,本文提出的浅海水深SAR遥感探测技术是收敛与可行的.     

西藏高原斜压对流边界层风、温、湿廓线特征

利用1998年夏季第2次青藏高原大气科学试验当雄观测站的边界层观测资料以及拉萨、改则和武汉等地探空资料,分析讨论西藏高原斜压对流边界层风、温、湿廓线的特征. 研究结果表明,高原地区白天对流边界层发展可高达2200m,显著超过中纬度平原地区和海面上对流边界层高度. 高原对流边界层中温度廓线具有较好的混合特征,湿度廓线有时在某一高度上出现湿度极大值. 高原对流边界层内热量和水汽收支分析表明,水平平流作用对边界层结构具有重要作用. 在对流边界层中平均风速垂直分布存在风切变现象. 水平温度梯度形成较强的斜压性是形成边界层风切变的主要原因.     

SAR浅海水下地形遥感探测技术综述

SAR已成为浅海水下地形探测的重要技术手段之一.与传统浅海水下地形探测技术相比,SAR浅海水下地形遥感探测技术具有明显的经济效益.该水深探测技术通过对浅海水下地形SAR图像仿真模型的反演求解,从SAR图像中提取水下地形信息.本文回顾了SAR浅海水下地形遥感探测技术的不同数值模型和应用实例,并针对目前SAR浅海水下地形遥感探测技术存在的问题和今后研究方向进行了探讨和总结.     

非对称型强飓风中的准平衡流特征分析

本文在论述飓风发生发展生命史过程中平衡、准平衡和非平衡态动力学特征的基础上,应用PV-ω方法,对具有非轴对称和长时间强度维持特征的飓风Bonnie（1998）进行了反演诊断分析,结果表明：基于非线性平衡模式的平衡流能够描述飓风水平涡旋场的基本特征,而加入准平衡ω方程得到的准平衡流能反映边界层入流、高层出流、眼墙区的剧烈倾斜上升运动和眼心区域的下沉运动.准平衡流描述了具有较长生命史组织化过程的强对流系统,而与其相联系的辐散运动与涡度同量级,证明了飓风准平衡流场具有涡散运动共存的特征,但在边界层顶的入流急流区和高层出流区仍存在高度非平衡态的超梯度流.利用反演的准平衡流场分析发现,当由环境风场低层到高层存在顺切变时,飓风内中尺度对流带移动方向的左侧,有利于强对流单体的发展和新对流单体的形成,右侧则相反,同时强气旋式旋转流场的作用,使得对流单体形成后随基本气流传播至对流减弱区,造成了飓风非对称结构的形成和维持.     

ERS-2 SAR反演海洋风矢量的研究

SAR(Synthetic Aperture Radar)反演海洋风矢量是当今微波遥感领域非常有意义的前沿课题. 本文首先介绍了星载SAR估算海面风向、风速的基本原理和三种主流反演算法，接着给出反演的流程图以及重要步骤. 然后，以2002年5月7日香港地区ERS-2 SAR海洋图像为例，对经典的SWDA (SAR Wind Direction Algorithm)－谱分析方法加以改进，求得具有180°模糊度的风向，并用香港天文台气象浮标实测数据消除了风向不确定性. 最后，利用CMOD4 GMF（Geophysical Model Function，地球物理模式函数）计算得到海面上10m高的风速. 与气象浮标站实测资料相比，利用ERS-2 SAR图像获取的海面风向、风速的精度均较高. 这一结果表明：如果对SAR预先进行ADC(Analog to Digital Converter)改正以及精确校准，结合改进的SWDA和CMOD4，可以获得高精度的风矢量.     

大气边界层研究进展

大气边界层对云和对流的发展、演变有重要作用.本文回顾了在大气边界层高度计算方法,边界层的时空分布特征、结构和发展机理,以及边界层参数化方案等方面的主要研究进展.大气边界层高度计算方法主要分为基于大气廓线观测数据计算和基于模式参数化方案计算两大类;大气边界层高度频率分布形态具有明显的日变化特征,并且稳定、中性和对流边界层高度的频率分布呈现出不同的Gamma分布特征;地面湿度状况对边界层发展影响明显,对于不同的下垫面热力性质和地形状况,大气边界层高度呈现出明显的空间差异,青藏高原边界层高度明显高于一般平原地区;在强烈的地面加热驱动下,对流边界层与残余层通过正反馈机制循环增长可以形成4000 m以上的超高大气边界层;研制大气边界层、浅对流以及云物理方案的统一参数化框架是未来数值预报模式的发展趋势.     

星载SAR海洋内波遥感研究进展

星载SAR已成为海洋内波研究的重要技术手段之一.本文回顾了SAR海洋内波遥感研究进展,特别是有关国内外SAR海洋内波的遥感成像机理研究、遥感成像仿真研究和遥感探测研究的发展,同时针对目前SAR海洋内波遥感研究存在的问题和今后有待研究的方向进行了探讨.     

基于星载SAR数据的台风参数估计及风场构建

传统的星载SAR数据海面风场反演方法是利用海面风场与雷达后向散射系数之间的经验关系即CMOD5模式函数求解海面风场.但在台风条件下,由于降雨对雷达信号的影响及高风速条件下CMOD5模式函数的停滞效应,海面风场的反演精度迅速下降.针对降雨对雷达信号的影响,本文基于星载SAR卫星平台未搭载降雨测量载荷的特点,将多时次的静止气象卫星红外云图用于推导台风云系的运动矢量,并由该运动矢量及非同步观测降雨数据估算星载SAR数据过境时的降雨强度.最后,利用订正模型和降雨强度数据进行降雨订正.针对高风速条件下CMOD5模式函数的停滞效应,本文基于台风的SAR图像特征和改进的HOLLAND台风模型,提出了台风参数估计及风场构建方案.首先,利用基于小波分析的风向提取算法提取台风风场的海面风向信息,并通过地球物理模式函数和风向信息反演海面风速.然后,根据台风眼的SAR图像特征计算台风中心位置和最大风速半径,并将其代入改进的HOLLAND台风模型.最后,利用中低风速数据通过最小二乘法拟合台风中心气压和最大风速,并将台风风向、中心位置、最大风速半径、中心气压和最大风速等参量代入改进的HOLLAND模型构建台风海面风场.为了验证方案的精度,选择台风"艾利"、"卡努"和"奥菲利娅"的星载SAR数据进行试验,并利用美国联合台风预警中心和飓风研究中心的最佳路径数据和风场数据进行精度检验.结果表明,本文利用星载SAR数据估算的台风中心位置、中心气压、最大风速与最佳路径数据基本一致,构建的海面风场精度较高,其中,海面风速的均方差为1.4 m s-1,风向的均方差为2.1°,为台风监测提供了新的技术途径.     

对流边界层顶部特性的对流槽实验模拟研究

利用对流槽研究对流边界层的顶部特性.实验结果表明,产生于混合层的上冲热泡可在对流边界层顶上的覆盖逆温层中激发出重力波;夹卷层的湍流结构表现出各向异性,水平尺度大于垂直尺度,与混合层中的湍流结构明显不同;利用可视图像直观显示了夹卷过程,夹卷层的温度谱表现出独特的结构特征,湍流能谱有明显的分区现象,谱幂率与现有理论分析结果有较大偏离.在实验结果的基础上,提出了关于夹卷速率的新参数化方案,夹卷速率可由地面热通量、混合层高度和覆盖逆温强度确定,方案中的系数C由实验测量数据拟合得出:C=0.95,与Deardroff等的对流槽实验数据的拟合结果(C=1.11)非常接近.     

基于拉格朗日分解算法的SAR图像混合像元分解

为解决与光学遥感图像不同的合成孔径雷达(SAR)图像中存在大量混合像元的问题,本文提出了一种基于拉格朗日分解算法的SAR图像混合像元分解的方法,结合相关内容中具体定理的证明,文中给出拉格朗日分解算法用于SAR图像混合像元分解的系统的求解方法.用人工模拟SAR图像和ENVISAT SAR图像进行实验,结果表明拉格朗日分解算法的混合像元分解结果明显优于非约束类神经网络(文中实验以BP神经网络为例)的分解结果.     

海面有效辐射的数值分析

本文基于大气辐射的基本概念和原理,对海面有效辐射进行分析讨论。首先,根据近海面大气边界层中的气温和湿度廓线跟风速廓线的相似性,采用海面粗糙参数z_0来定义海面。其次,由海面有效辐射的定义和大气辐射理论导出海面有效辐射的一般表达式。然后,对海洋大气的垂直结构作了分层描述,从而对海面有效辐射一般表达式进行具体运算,并且求得简化分析式。最后,利用海洋观测站资料,对本分析式和一些经验公式进行计算和对比。结果表明,晴天与阴天的海面有效辐射值相差较大,可是它们随海面风速的变化均甚小。     

The retrieval of two-dimensional distribution of the earth''''s surface aerodynamic roughness using SAR image and TM thermal infrared image

The research for the land surface fluxes has madea quiet great progress for its breakthroughs in the fieldof regional or global interactions between land surfaceand atmosphere. However, many remote sensing mod-els for estimating the land surface fluxes need the pa-rameters of surface momentum, heat, resistance ofwater vapor at a referenced height, which are the func-tion of aerodynamic surface roughness zad. It hasbeen validated that the retrieval of the land surfacefluxes is very sensitive to…     

Air–sea interactions during strong winter extratropical storms

A high-resolution, regional coupled atmosphere–ocean model is used to investigate strong air–sea interactions during a rapidly developing extratropical cyclone (ETC) off the east coast of the USA. In this two-way coupled system, surface momentum and heat fluxes derived from the Weather Research and Forecasting model and sea surface temperature (SST) from the Regional Ocean Modeling System are exchanged via the Model Coupling Toolkit. Comparisons are made between the modeled and observed wind velocity, sea level pressure, 10 m air temperature, and sea surface temperature time series, as well as a comparison between the model and one glider transect. Vertical profiles of modeled air temperature and winds in the marine atmospheric boundary layer and temperature variations in the upper ocean during a 3-day storm period are examined at various cross-shelf transects along the eastern seaboard. It is found that the air–sea interactions near the Gulf Stream are important for generating and sustaining the ETC. In particular, locally enhanced winds over a warm sea (relative to the land temperature) induce large surface heat fluxes which cool the upper ocean by up to 2 °C, mainly during the cold air outbreak period after the storm passage. Detailed heat budget analyses show the ocean-to-atmosphere heat flux dominates the upper ocean heat content variations. Results clearly show that dynamic air–sea interactions affecting momentum and buoyancy flux exchanges in ETCs need to be resolved accurately in a coupled atmosphere–ocean modeling framework.     

Indirect air–sea interactions simulated with a coupled turbulence-resolving model

A turbulence-resolving parallelized atmospheric large-eddy simulation model (PALM) has been applied to study turbulent interactions between the humid atmospheric boundary layer (ABL) and the salt water oceanic mixed layer (OML). The most energetic three-dimensional turbulent eddies in the ABL–OML system (convective cells) were explicitly resolved in these simulations. This study considers a case of shear-free convection in the coupled ABL–OML system. The ABL–OML coupling scheme used the turbulent fluxes at the bottom of the ABL as upper boundary conditions for the OML and the sea surface temperature at the top of the OML as lower boundary conditions for the ABL. The analysis of the numerical experiment confirms that the ABL–OML interactions involve both the traditional direct coupling mechanism and much less studied indirect coupling mechanism (Garrett Dyn Atmos Ocean 23:19–34, 1996). The direct coupling refers to a common flux-gradient representation of the air–sea exchange, which is controlled by the temperature difference across the air–water interface. The indirect coupling refers to thermal instability of the Rayleigh–Benard convection, which is controlled by the temperature difference across the entire mixed layer through formation of the large convective eddies or cells. The indirect coupling mechanism in these simulations explained up to 45 % of the ABL–OML co-variability on the turbulent scales. Despite relatively small amplitude of the sea surface temperature fluctuations, persistence of the OML cells organizes the ABL convective cells. Water downdrafts in the OML cells tend to be collocated with air updrafts in the ABL cells. The study concludes that the convective structures in the ABL and the OML are co-organized. The OML convection controls the air–sea turbulent exchange in the quasi-equilibrium convective ABL–OML system.     

Turbulence structure of the boundary layer below marine clouds in the SOFIA experiment

The SOFIA (Surface of the Ocean: Flux and Interaction with the Atmosphere) experiment, included in the ASTEX (Atlantic Stratocumulus Transition EXperiment) field program, was conducted in June 1992 in the Azores region in order to investigate air-sea exchanges, as well as the structure of the atmospheric boundary layer and its capping low-level cloud cover. We present an analysis of the vertical structure of the marine atmospheric boundary layer (MABL), and especially of its turbulence characteristics, deduced from the aircraft missions performed during SOFIA. The meteorological situations were characteristic of a temperate latitude under anticyclonic conditions, i.e., with weak to moderate winds, weak surface sensible heat flux, and broken capping low-altitude cloud cover topped by a strong trade inversion. We show that the mixed layer, driven by the surface fluxes, is decoupled from the above cloud layer. Although weak, the surface buoyancy flux, and the convective velocity scale deduced from it, are relevant for scaling the turbulence moments. The mixed layer then follows the behavior of a continental convective boundary layer, with the exception of the entrainment process, which is weak in the SOFIA data. These results are confirmed by conditional sampling analysis, which shows that the major turbulence source lies in the buoyant moist updrafts at the surface.     

Sea Ice Dynamics Induced by External Stochastic Fluctuations

The influence of stochastic fluctuations in the atmosphere and in the ocean caused by different occasional phenomena (noises) on dynamic processes of sea ice growth with a mushy layer is studied. It is shown that atmospheric temperature variances substantially increase the sea ice thickness, whereas dispersion variations of turbulent flows in the ocean to a great extent decrease the ice content produced by false bottom evolution.     

Implications of Warm Rain in Shallow Cumulus and Congestus Clouds for Large-Scale Circulations

Space-borne observations reveal that 20–40% of marine convective clouds below the freezing level produce rain. In this paper we speculate what the prevalence of warm rain might imply for convection and large-scale circulations over tropical oceans. We present results using a two-column radiative–convective model of hydrostatic, nonlinear flow on a non-rotating sphere, with parameterized convection and radiation, and review ongoing efforts in high-resolution modeling and observations of warm rain. The model experiments investigate the response of convection and circulation to sea surface temperature (SST) gradients between the columns and to changes in a parameter that controls the conversion of cloud condensate to rain. Convection over the cold ocean collapses to a shallow mode with tops near 850 hPa, but a congestus mode with tops near 600 hPa can develop at small SST differences when warm rain formation is more efficient. Here, interactive radiation and the response of the circulation are crucial: along with congestus a deeper moist layer develops, which leads to less low-level radiative cooling, a smaller buoyancy gradient between the columns, and therefore a weaker circulation and less subsidence over the cold ocean. The congestus mode is accompanied with more surface precipitation in the subsiding column and less surface precipitation in the deep convecting column. For the shallow mode over colder oceans, circulations also weaken with more efficient warm rain formation, but only marginally. Here, more warm rain reduces convective tops and the boundary layer depth—similar to Large-Eddy Simulation (LES) studies—which reduces the integrated buoyancy gradient. Elucidating the impact of warm rain can benefit from large-domain high-resolution simulations and observations. Parameterizations of warm rain may be constrained through collocated cloud and rain profiling from ground, and concurrent changes in convection and rain in subsiding and convecting branches of circulations may be revealed from a collocation of space-borne sensors, including the Global Precipitation Measurement (GPM) and upcoming Aeolus missions.     

Modeling studies of the upper ocean response to a tropical cyclone

A coupled ocean and boundary layer flux numerical modeling system is used to study the upper ocean response to surface heat and momentum fluxes associated with a major hurricane, namely, Hurricane Dennis (July 2005) in the Gulf of Mexico. A suite of experiments is run using this modeling system, constructed by coupling a Navy Coastal Ocean Model simulation of the Gulf of Mexico to an atmospheric flux model. The modeling system is forced by wind fields produced from satellite scatterometer and atmospheric model wind data, and by numerical weather prediction air temperature data. The experiments are initialized from a data assimilative hindcast model run and then forced by surface fluxes with no assimilation for the time during which Hurricane Dennis impacted the region. Four experiments are run to aid in the analysis: one is forced by heat and momentum fluxes, one by only momentum fluxes, one by only heat fluxes, and one with no surface forcing. An equation describing the change in the upper ocean hurricane heat potential due to the storm is developed. Analysis of the model results show that surface heat fluxes are primarily responsible for widespread reduction (0.5°–1.5°C) of sea surface temperature over the inner West Florida Shelf 100–300 km away from the storm center. Momentum fluxes are responsible for stronger surface cooling (2°C) near the center of the storm. The upper ocean heat loss near the storm center of more than 200 MJ/m² is primarily due to the vertical flux of thermal energy between the surface layer and deep ocean. Heat loss to the atmosphere during the storm’s passage is approximately 100–150 MJ/m². The upper ocean cooling is enhanced where the preexisting mixed layer is shallow, e.g., within a cyclonic circulation feature, although the heat flux to the atmosphere in these locations is markedly reduced.     

Effects of wind shear on the atmospheric convective boundary layer structure and evolution

The article reviews past accomplishments and recent advances in conceptual understanding, numerical simulation, and physical interpretation of the wind shear phenomena in the atmospheric convective boundary layer.