## 1 Introduction  
Studying the seismic structures and spatiotemporal relationships of two or more large (\(\mathbf{M}\geq 7.0\)) intraplate earthquakes that occurred in close spatial proximity within a short period of time is important [1; 2; 3; 4; 5]. The Sumatran Fault in western Indonesia has produced multiple \(\mathbf{M}\mathbf{w}\geq 7.0\) earthquakes in the last century [6]. The seismic structures that produced the 2008 Wenchuan _Ms_ 8.0 and 2013 Lushan _Ms_ 7.0 earthquakes are both related to those of the Longmenshan Fault; however, these two earthquakes were independent rupture events in the middle and southern segments of the Longmenshan Fault, respectively [1; 6]. Similarly, the 2023 Turkey _Mw_ 7.8 earthquake triggered activity on its northern side, which caused a _Mw_ 7.5 earthquake on the Cardak-Surgu Fault [7; 8]. As shown by these examples,understanding the relationships between adjacent large earthquakes is crucial for seismic hazard analysis and assessment. The Shanxi Graben is located in the central part of the North China Craton, situated between the Ordos and North China Block. This area features a series of NNE-trending fault basins [9; 10; 11] (Figure 1) and is an important part of the fault system around the Ordos Block [12; 13]. Current GPS observation data show that the blocks on both sides of the Shanxi Graben rotate counterclockwise, and the Shanxi Graben is located in a strong right-lateral strike-slip stress concentration area and strain zone [12; 14]. Historical records reveal the occurrence of several strong earthquakes in the region (Figure 1) [9; 15; 16; 17; 18]. The 1303 Hongtong \(M\) 8 and 1695 Linfen \(M\) 7.8 earthquakes occurred in the Linfen Basin, in the southern part of the Shanxi Graben [19; 20; 21]. The seismically active area exhibits extensive Quaternary deposits [15; 22; 23]. Previous studies suggest that the faults in this area have a low slip rate [12; 14; 24] and a long earthquake recurrence interval [25; 26]. A comprehensive analysis of the tectonics and the seismogenic environment associated with the two large earthquakes in the Linfen Basin, using geophysical data such as seismic reflection profiles and velocity structures, and the development of a reasonable three-dimensional seismo-tectonic model are essential for understanding the dynamic mechanisms of earthquakes. On 17 September 1303, the Hongtong \(M\) 8 earthquake occurred in the Linfen Basin. This event was followed by several significant aftershocks over the subsequent years, resulting in more than 200,000 deaths [27; 28; 29; 30; 31]. Most current studies consider the Huoshan Fault as the seismogenic fault of the Hongtong earthquake (Figure 2a) [32; 33]. On 18 May 1695, 392 years after the Hongtong earthquake, a large earthquake occurred again in the Linfen Basin, only 45 km away from the epicentre of the Hongtong earthquake, causing more than 50,000 deaths [34]. There are different beliefs regarding the seismogenic faults of the Linfen \(M\) 7.8 earthquake. Some studies consider the Guojiazhuang Fault (F5) near the epicentre as the seismogenic fault of the Linfen \(M\) 7.8 earthquake (Figure 2a) [35; 36; 37]. However, some studies show that the scale of the Guojiazhuang Fault is not sufficient to cause the Linfen \(M\) 7.8 earthquake [38]. Thus, the seismogenic faults of the Linfen earthquake remain unclear. Additionally, current studies on the Hongtong and Linfen earthquakes primarily focus on geological surveys of surface faults, with insufficient analysis of deep structures. Therefore, analysing the deep seismogenic environment, relationships, and seismogenic tectonic model of these two major earthquakes is important for assessing potential seismic hazards in the Linfen area.