This is the necessary and initial step to build a dynamic model. Judging from the sequence of magmatic-tectonic events and the division of orogenic curtains, whether it is the scale of an orogenic curtain or the whole orogenic process, it records the process that the continental crust is first heated, then thickened by contraction structures, and finally lifted and eroded. Therefore, it has a CCW)PTt trajectory (Figure 2-79). Therefore, in general, the lithosphere is thin (60 ~ 100 km) and the continental crust is thick (55 ~ 60 km), which is similar to the lithosphere structure of the Andes and Gangdise mountains today.
Fig. 2-79 schematic diagram of PTt trajectory in Yanshan period of North China.
In thermal simulation, the uplift of the continental crust after instantaneous thickening is about 100 ~ 120 Ma (see section 1). However, the continental crust uplift after the thickening of the North China orogenic belt is only a few Ma, or even ≤ 1Ma. Therefore, it is impossible for the thickened continental crust to return to the thickness before thickening and suffer another contraction structure. As a result, over time,
(2) Dynamic model of Yanshan orogenic belt
Based on the existing model (Wu Fuyuan et al., 2003, Deng et al., 2003) and the PTt trajectory of orogeny, an improved dynamic model (Figure 2-80) can be constructed, which can be summarized as follows: ①J 1 and the lithosphere that broke twice along the lithosphere, and basaltic magma invaded the bottom of the crust and broke deeply (L 1). ② The second contraction structure in late J1and late J2 thickened the continental crust, and at the same time basaltic rocks and ultramafic rocks that had infiltrated into magma chamber were transformed into eclogites, which transformed the original craton lithosphere (L 1) into a compact lithosphere (L2), resulting in the lithosphere sinking (Figure 2-80b); ③ The subsidence and extension of J3 and K 1 1 high-density lithosphere (L2) caused the eclogite in Moho structural weak zone and piedmont zone to rupture nearly horizontally along the top boundary, which eventually led to the subsidence of lithosphere and the upwelling of asthenosphere, leading to the eruption of regional basaltic magma (Figure 2-80c); ④K2 1 Due to the termination of the regional compressive stress field, the continental crust of Jushangen uplifted, leading to the extensional structure after orogeny. At this time, the asthenosphere began to cool and gradually became a new lithosphere (L3). Due to the cooling of the asthenosphere, volcanism basically stopped, and only post-orogenic intrusion activities developed (Figure 2-80d). It can be seen that the model in Figure 2-80 shows that the extension of post-orogeny is mainly caused by the stop of regional compression position and severe crustal uplift. At this time, it is not a large-scale detachment of the lithosphere, but a process in which the asthenosphere begins to cool and gradually transforms into a new lithosphere, and the disturbed L/A system moves towards stability.
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