Eastern Eurasia have experienced large-scale and long-term intra-continental deformation in the Cenozoic (Tapponnier et al., 2001;Yin, 2010). The continental deformation in eastern Eurasia is manifested by mountain building (e.g., the growth of the Qinling and Liupanshan mountains) (Yin, 2010), reactivation of large strike-slip shear zones that stretch thousands of kilometers from west to east (e.g., the Qilian and Qinling faults) (Enkelmann et al., 2006;Tapponnier et al., 1990), development of localized rifting systems from northern Tibet to the Trans North China Craton (TNCO) (e.g., the Weihe and Shanxi rifts and South Ningxia-Yinchuan-Hetao basin) (Zhang et al., 1998), and volcanism in the intraplate settings (e.g., the Fansi, Datong, and Hebi volcanoes) (Xu, 2007) (Figure 1a).The Ordos block and Sichuan basin have thick cratonic keels and are considered to be the cores of eastern Eurasian continent. They are often viewed as barriers that divide eastern Eurasia into two broad intra-continental deformation regimes. To the west, the indention of the Indian continent to the Eurasian continents since ∼50 Ma has led to a total of ∼1,000-2,000 km north-south shortening of the Eurasian continent, resulting in the high topography within the Tibetan interior and over 250-1,250 km eastward continent expansion (Molnar & Tapponnier, 1975). In contrast, the tectonic evolution of eastern margins of Eurasia is subject to the subduction and subsequent retreat of the western Pacific plate. The eastern Eurasia is predominated by extensional deformation, manifested