**4. Real Data Application**

The proposed method is then applied to field data acquired in northern China. The Q−<sup>1</sup> results are calculated using logging data by the pore fluid dissolution model. Figure 10a shows the Q−<sup>1</sup> results at 60 Hz of this model in the depth from 1500 m to 2500 m. The results match well with the Q−<sup>1</sup> measurements from the core data. The velocity is then upscaled by the SLS model. Figure 10b shows the well-to-seismic calibration before and after using velocity dispersion results from the SLS method as guidance for stretching the events. The event at 1900 ms is fixed, and the event at 1820 ms is stretched 5 ms. The event at 1740 ms is stretched 8 ms with the event at 1820 ms fixed. The corresponding velocity dispersion is calculated as roughly 7% and 4%, which is consistent with that of the SLS model. The upscaled velocity is useful for well-to-seismic calibration and makes the correction more reasonable.

**Figure 10.** (**a**) Comparison of Q−<sup>1</sup> results by the WIGED model using logging data and data from core measurements. (**b**) Well-to-seismic calibration before and after using Q−<sup>1</sup> results from the WIGED method as a guidance.
