印度洋偶极子（Indian Ocean Dipole，简称IOD）作为热带印度洋上一个重要的海气耦合系统，对局地乃至全球的天气、气候变化都有着非常重要的影响。前人关于IOD动力过程研究主要集中在热带印度洋表层次表层部分，作为重要的下垫面外源强迫，其与大气环流的变化有着密切关系，而热带印度洋区域非绝热加热影响区域环流系统动能的变化和机理尚不清楚。本文利用现有的再分析资料，借助克服传统有效位能的局限性提出的局地大气扰动位能理论，对局地动能的变化进行研究，发现扰动位能在联接非绝热加热和局地动能之间起到重要的纽带作用。通过计算IOD期间大气扰动位能、动能以及扰动位能与动能的转化项等物理量，从新的局地能量学的角度探究了IOD事件中，热带印度洋上空对流层大气扰动位能的时空变化特征、能量转换以及对局地大气环流的影响过程，得到了以下主要结论： （1）揭示了IOD期间印度洋东西极海温变化显著的负相关关系，西极海温存在一个对东极海温变化的延迟效应。且大气扰动位能对海温异常有着快速的响应。海温负异常首先从印度洋东极开始，冷的海温会使得输送的能量减少，扰动位能同时表现为负异常。随后印度洋西极出现海温正异常，使得海洋向大气输送的能量增加，扰动位能表现为正异常，对于对流层低层而言，大气扰动位能的变化与海温变化在时空上较为一致；在中高层大气，大气扰动位能的变化具有一定的时滞性，这是由于能量从低层向高层的传输需要一定的时间，同时强度有一定的衰减。所以整层的扰动位能变化主要受低层控制，是大气对海温响应的主体。 （2）发现了IOD期间大气扰动位能对于联接关键区海温影响大气动能变化中起到的纽带作用。海温指数与扰动位能指数呈现明显的正相关，关键区动能同时与二者表现为负相关关系，说明海温异常可以通过非绝热加热对大气的扰动位能产生影响，然后扰动位能又进一步通过能量转化影响动能，对印度洋区域的大气运动产生影响，扰动位能在其中起到纽带的作用。同时在IOD的发展过程中，能量在大气扰动位能与动能转化呈明显的东西偶极子分布，反向的能量转化过程对环流的异常变化有着不同的影响，然后异常的环流通过海气进一步的相互作用再影响海温。 （3）阐明了在IOD的发展阶段，热带印度洋对流层扰动位能的变化会引起大气能量转化的异常，进而调整局地Walker环流过程的物理机制。由于东极转化项的增强，可以转化为动能的部分减少，东极低层动能辐散加强，环流减弱，低层东风发展，而西极转化项主要表现为负异常，表示可以转化为动能的部分增加，西极低层动能辐合加强，Walker环流进一步减弱，东风得到加强。IOD的东、西两极的能量转换过程为IOD演化的发展和加强过程提供了正反馈过程。

As an active coupled ocean-atmosphere system, the Indian Ocean Dipole (IOD) plays a significant role on the regional or even global weather and climate events. Previous researches mainly focus on the dynamic processes of sub-surface and surface water in the tropical Indian Ocean. However, tropical atmospheric energy changes during the IOD events are given less attention. In this paper, the evolution of the atmospheric layer perturbation potential energy (PPE) over the tropical Indian Ocean is analyzed in a composite IOD event using reanalysis datasets for the period 1848–2015. PPE is closely related to both SST and kinetic energy during the IOD and PPE is the key link between underlying external forcing and KE. The variation of PPE is modulated by IOD, and then affect KE through energy conversion. The PPE anomalies in the lower troposphere (1000–850 hPa) are the dominant layers of the PPE in the whole troposphere(1000–150 hPa) showing a dipole pattern corresponding to the anomalous variation of surface sea temperature (SST) and are more significant than those in the middle–upper troposphere (600–200 hPa) during the IOD event. During the IOD event, PPEAs in the lower troposphere (1000–850 hPa) show a dipole pattern in response to the SSTAs and the evolution is basically synchronous with SSTAs. Negative PPEAs and SSTAs occurs firstly in the IOD-E. Along with the SSTAs intensify in the Indian Ocean, PPEAs develop into a noticeable dipole pattern over the tropical Indian Ocean from July to August. Then, negative PPEAs weaken over the IOD-E and positive PPEAs expand eastwards covering the entire Indian Ocean. The change of PPE in the middle–upper troposphere lags to the lower troposphere. PPEAs of whole troposphere (1000–150 hPa) have the strongest response part in the lower layer of the troposphere and have the similar features to the PPEAs in the lower troposphere (1000–850 hPa). During the IOD event, there is a “delayed effect” for IOD-W SST to IOD-E SST. The correlations between U-wind and SSTAs in two poles suggest that the U-wind may cause the “delayed effect” through the air-sea interaction and the PPE has important impact on the U-wind during the IOD through the energy conversion. When CK is positive in the IOD-E, there are less PPEAs can convert into KE, atmospheric KE decreases, weakening the lower level convergence of the climatological Walker circulation over the IOD-E and the surface anomalous easterly wind develop making along the west coast of Sumatra to prevail and raising the coastal thermocline to be shallow, warmer SSTAs in the IOD-W begin to develop. On the other hand, the condition of PPEAs and CK over the IOD-W are opposite to the east and the anomalous easterly wind further continue developing and the positive SSTAs in the IOD-W peak.