## 5 Discussion
### Analysis of the Reliability of the Glacial Chronology of the EAM Region
[PERSON] [86] recorded the earliest glacial advance in Yulong Mountain as the 600-700 Ka Yulong glacial period (MIS16-18) measured by ESR dating, which is equivalent to the late Wangkun glacial period in the TP, indicating that the HD MTs began to enter the cryosphere during this period. In the mountains of the Asia inland area (AIA), the oldest measured glacial advance was found in the remnant moraine of Gaowang Peak (Tianshan Mountain), with ESR dating results of 459.7-477.1 ka [87], corresponding to the Zhonglianggan period. By comparing the glacial period/stage in the EAM region with those in western China, we found that there were significant differences between the extent, onset time and length of glacial periods (Figure 3). [PERSON] [14] studied the features of glaciations during the LGP in the EAM region and found that the MIS 6-5 glaciation first appeared in the coastal mountains of East Asia, indicating a strengthening glaciation. Conversely, in western China, where there were multiple glaciations, the extent of glacial ice gradually shrank. This phenomenon seems contradictory, but in fact, small East Asian coastal and island mountains only approached or reached their modern altitudes during the LGP as a result of strong neotectonic movement [88]. However, due to the uplift of the TP, the mountains in western China highly inhibited any potential climatic impact, restricting early glacial advances during the LGP. We found that the earliest records of glacial advance were in the mountains of Japan and Taiwan. Both these mountainous areas are located in an island arc that has experienced the strongest tectonic uplift, as well as major volcanic and plate activity, Taiwan and Japan are both alpine glacier types. [PERSON] et al. [29] pointed out that the uplift rate of neotectonic movement since the LGP in the mountains of Taiwan was 5 mm/a; it has been calculated that the uplift of Mount Nanhutta since the LGM is \(\sim\)275 m, potentially related to the Gonghe Movement (150 ka) [49] (Figure 3). Therefore, if monsoonal fluctuations can be taken to affect the extent of any glaciation, tectonic movement may similarly be an important determinant of the history of a glacial period/stage, it has provided an absolute spatial height basis for the development of mountain glaciers. It needs to be emphasized that tectonic movement cannot completely explain the advance and retreat of mountain glaciers, because the tectonic uplift in different are significantly different. The same monsoon circulation environment changes are the main driving force for the overall change of mountain glaciers in the study area. Influence of EAM Circulations on Glacial Stages in the Mountains of the EAM Region during the Late Quaternary Glacial Period  
Current research suggests that changes in the intensity of the EAM were caused by changes in the Earth's orbital path [89]. The EAM's principal control appears to be the degree of summer solar radiation experienced in the high latitudes of the Northern Hemisphere, as caused by precession [90; 91]. The climatic evolution of the EAM therefore displays a clear Milankovitch cyclic pattern, with an orbital eccentricity of 100 ka, a plane tary axial tilt of 41 ka, an equinoctial precession of 23 ka, and periodic changes of 0.8 ka [92]. There is a telecorrelation between the Asian Monsoon and abrupt changes in sea surface temperatures (SSTs) and ice coverage in the North Atlantic [93]. The Early LGP in the EAM region was affected by the Greenland cold event in the North Atlantic [94], and the Heinrich event was characterized by weak monsoonal circulations [95]. The long-term evolution of the EAM is not only closely related to changes in global ice induced by solar radiation, but also to regional environmental changes such as land-sea changes, uplift of the TP, sea level fluctuations, and changes in the circulatory patterns of the Westerlies. It is a coupling process dependent upon many different factors [5].