## 2 Data and Methodology  
The data utilized in this study comprises basin formation pressure states, tectonic evolution histories, and tectonic movement rates from over 50 basins or regions both domestically and internationally. Additionally, measured data on organic and inorganic pores from 163 overpressured strata in 11 basins or regions were included, along with calculations of their respective proportions. The method of study is to analyze the pressure changes of stratigraphic water in the formation of sedimentary basins and the process of diagenetic evolution. In porous media, the water is smaller than other hydrocarbon molecules, and 3.2 A (1 A = 10-10 m), so there is water penetration in places with abnormal stress. The following Table 1 shows the effective diameter of different molecules [29]. Under the conditions of formation, the deeper the pressure, the local if there is a condition that exceeds the hydrostatic force condition, the water has the tendency to permeate and tend to the hydrostatic pressure. Although water has strong permeability, there is a certain lag time in strata of different lithologies, and the process is not instantaneously completed. According to the Poiseuille formula [30; 31], assuming a mudstone stratum thickness of 200 m and a pore radius of 2 nm, it only takes 1.5 Ma for the formation water in the reservoir to drop from an initial 2.6 times overpressure to 1.2 times overpressure due to the permeability of the mudstone, as shown in Table 2. [PERSON] (2024) [32] studied the pore size distribution of 7 shale samples from the Shahejie Formation in the Iiyama Depression and found that pores ranging from 0-4 nm accounted for 59%, indicating that this pore radius is reasonable. During rapid accumulation, the initial condition is that both the stratum and stratum framework bear the crustal stress together, so 2.6 is taken. This calculation can at least illustrate that the permeability of water in the stratum is relatively fast. During the syngenetic and early diagenetic stages, due to higher porosity and permeability coefficients, the formation pressure remains at hydrostatic pressure (normal pressure). The subsequent analysis in this article mainly focuses on strata in the middle and late diagenetic stages. \begin{table}
\begin{tabular}{c c c c} \hline
**Molecule** & **Effective Diameter Å** & **Molecule** & **Effective Diameter Å** \\ \hline H\({}_{2}\)O & 3.2 & C\({}_{3}\)H\({}_{8}\) & 5.1 \\ He & 2.0 & Benzene & 4.7 \\ CO\({}_{2}\) & 3.3 & Normal alkanes & width: 4.2 length: 4.2\(\sim\)-4.8 \\ N\({}_{2}\) & 3.4 & Cyclohexane & 5.4 \\ CH\({}_{4}\) & 3.8 &
\begin{tabular}{c} Complex cyclic \\ compounds \\ \end{tabular} & 15\(\sim\)20 \\ C\({}_{2}\)H\({}_{6}\) & 4.4 & Bitumen & \(>\)50 \\ \hline \end{tabular}
\end{table} 
Table 1: Effective of different molecules (Unit: Å). A set of regional cap rocks with certain sealing properties may contain multiple lithologies, such as thick shale, gypsum-salt rock, and thin sand layers. To maintain overpressure in the formation itself or its underlying sandstone reservoir, it is necessary to calculate the time required for pressure relief. The calculation can be approximated by the following formula:  
\[t\ =\ A\sum_{i\ =\ 1}^{n}\frac{S_{S}h_{i}^{2}}{K_{i}} \tag{1}\]  
In the formula, \(t\) represents the required time (s), \(h_{i}\) is the thickness of each sublayer (m), and \(K_{i}\) is the permeability coefficient of each sublayer (m/s). The \(Ss\) represents the water storability (1/m). \(A\) represents the dissipation coefficient, which can be taken as 1.5. Moreover, \(n\) represents the number of layers. According to [PERSON] et al. (2024), the \(Ss\) can be taken as 0.0008 [33]. Based on the research by [PERSON] et al. (2008) [34], the permeability coefficient of mudstone caprock can be taken as 4 \(\times\) 10\({}^{-12}\) m/s. Calculating separately for caprock thicknesses of 100 m, 200 m, 300 m, and 500 m, the required time for abnormal pressure release in the strata is approximately 0.23 Ma, 0.9 Ma, 2.1 Ma, and 5.71 Ma.