The frequently observed tropospheric warm cores over the Tibetan Plateau (TP) are unique climate phenomena and are crucial to the Asian summer monsoon development. However, their climatological structure and formation mechanisms remain elusive and inconsistent among previous studies. In this work, two vertically separated warm cores, the upper-level warm cores (ULWCs) and lower-level warm cores (LLWCs), are identified based on the zonal temperature deviation. The LLWCs are basically confined below 450 hPa, and the ULWCs are mostly observed at 200–400 hPa. The active region of the LLWCs is generally within the TP domain and characterized by regional patches with high frequency occurrences. In contrast, the active region of the ULWCs is featured by a zonally elongated band along the southern TP. The physical mechanisms for the formations of these two distinct types of warm cores are revealed: the LLWCs are mainly generated and maintained by the surface diabatic heating, while the ULWCs are dominated by the large-scale circulation associated with the convection over the Indo-Pacific warm pool. During March–June, the ULWCs within the TP domain occur most frequently and the intensities attain their maxima. In March–April, the ULWCs are mainly determined by the TP adiabatic subsidence induced by the convection over the Indo-Pacific warm pool. In May–June, the warm advection induced by westerlies generates the downstream ULWCs and enhances the ULWCs formed in previous months. Hence it might be inappropriate in traditional view to attribute the tropospheric warm cores around the TP solely to the direct thermal effect of the elevated topography.

青藏高原（TP）上经常观测到的对流层暖芯是独特的气候现象，对于亚洲夏季风的发展至关重要。然而，在先前的研究中，它们的气候结构和形成机制仍然难以捉摸且不一致。在这项工作中，根据区域温度偏差确定了两个垂直分开的暖心，即上层暖心（ULWC）和下层暖心（LLWC）。LLWC基本上被限制在450 hPa以下，而ULWC大多在200–400 hPa处观察到。LLWC的活动区域通常在TP域内，其特征是出现高频信号的区域性斑块。相比之下，ULWCs的活动区域以沿着南部TP的带状拉长带为特征。揭示了形成这两种不同类型的暖核的物理机制：LLWC主要是由地表非绝热加热产生和维持的，而ULWC则主要是由与印度太平洋对流有关的大规模环流所主导的。温暖的游泳池。在3月至6月期间，TP域内的ULWC最频繁发生，并且强度达到最大值。在三月至四月，超高空速主要由印度洋-太平洋暖池对流引起的总热绝热沉降决定。在5月至6月，由西风引起的热对流产生了下游ULWC，并增强了前几个月形成的ULWC。因此，传统观点认为将对流层周围的对流层暖核仅归因于地形升高的直接热效应可能是不合适的。