At present, the fault sliding speed functions, or source time functions that used in theoretical seismogram calculation are all theoretical results. That is, the fault speed time functions are the results of the theoretical study, and they are not proved by the measured data. The method that used to calculate fault sliding speed by using Doppler effect has been greatly improved in this paper from the following four perspectives: Firstly, the paper proves theoretically how to confirm the seismic waves that received in some frequency bands by two receivers are emitted by the same source. Secondly, the paper puts forward the method to make sure whether seismic waves received by two receivers in some frequency bands are similar by using relative change of Fourier amplitude standard deviation in some frequency bands of two receivers, and similar seismic waves are emitted by the same frequency bands. Thirdly, to eliminate the interference of reflection and refraction waves, S wave records in fault sliding time are selected for data processing. Finally, long time Fourier transform is replaced by short time Fourier transform (STFT) to enhance fault sliding time positioning accuracy. On the basis of the work above, a general method to calculate the fault sliding speed by using Doppler effect is summarized systematically. The fault sliding speed of Wenchuan earthquake is calculated by the method mentioned above. The calculations show that Wenchuan earthquake fault sliding speeds are basically consistent with the seismic moment changes. It has proved that the sliding speed of Wenchuan earthquake fault has the characteristics of abrupt change, that is, the sliding speed increases suddenly and decreases rapidly. For most of the time, the sliding speed is not large, and sometimes the fault does not slide. There are obvious differences from sliding speed functions that are applied currently, such as Haskell function, Bell shaped functions, Exponential function, Triangle function, etc. To compute fault sliding speed by using Doppler effect, instead of grasping so-far unknown crust parameters, we only need to know the earthquake records, the locations of the epicenter and the receivers. In a word, the calculation method has clear physical meaning and the parameters required are easier to be obtained.

目前，理论地震图计算中使用的断层滑动速度函数或震源时间函数均为理论结果。就是说，故障速度时间函数是理论研究的结果，实测数据没有得到证实。本文从以下四个方面对使用多普勒效应来计算断层滑动速度的方法进行了很大的改进：首先，本文从理论上证明了如何确定两个接收机在某些频段接收到的地震波是如何发射的。相同的来源。其次，提出了利用两个接收机在某些频段上的傅立叶幅度标准偏差的相对变化来确定两个接收机在某些频段上接收到的地震波是否相似的方法，相同的频带发出相似的地震波。第三，为消除反射波和折射波的干扰，选择断层滑动时间内的S波记录进行数据处理。最后，将长时傅立叶变换替换为短时傅立叶变换（STFT），以提高故障滑动时间的定位精度。在上述工作的基础上，系统总结了利用多普勒效应计算故障滑动速度的一般方法。利用上述方法计算出汶川地震的断层滑动速度。计算表明，汶川地震断层滑动速度与地震矩变化基本吻合。事实证明，汶川地震断层的滑动速度具有突变的特征，即 滑动速度突然增加并迅速减小。在大多数情况下，滑动速度并不大，有时故障也不会滑动。与当前应用的滑动速度函数有明显的差异，例如Haskell函数，Bell形函数，指数函数，三角函数等。要使用多普勒效应来计算故障滑动速度，而不是掌握迄今为止未知的地壳参数，我们只需要知道地震记录，震中和接收者的位置。简而言之，该计算方法具有明确的物理含义，并且更容易获得所需的参数。与当前应用的滑动速度函数有明显的差异，例如Haskell函数，Bell形函数，指数函数，三角函数等。要使用多普勒效应来计算故障滑动速度，而不是掌握迄今为止未知的地壳参数，我们只需要知道地震记录，震中和接收者的位置。简而言之，该计算方法具有明确的物理含义，并且更容易获得所需的参数。与当前应用的滑动速度函数有明显的差异，例如Haskell函数，Bell形函数，指数函数，三角函数等。要使用多普勒效应来计算故障滑动速度，而不是掌握迄今为止未知的地壳参数，我们只需要知道地震记录，震中和接收者的位置。简而言之，该计算方法具有明确的物理含义，并且更容易获得所需的参数。