Full-waveform inversion (FWI), which is among the most powerful seismic data processing techniques for imaging subsurface geological structures, has a huge computational cost in proportion to the number of sources. To increase the speed of FWI, we explored the use of common-receiver gathers (CRGs) as an alternative to common-shot gathers (CSGs) as observed data. This approach has the potential to reduce the computational cost of FWI significantly, particularly for ocean-bottom cable (OBC) acquisition. As we match modelled and observed CSGs in CSG-based FWI, we match observed CRGs with modelled CSGs of switched source–receiver geometry in CRG-based FWI. According to the reciprocity principle, CRG FWI based on the steepest descent or Gauss–Newton method yields the same inverted velocity models as CSG FWI for an identical and known source signature applied over whole source positions. However, when the source wavelet is unknown, and changes from one source position to another, each trace of a CRG contains a different source signature, making it difficult to apply conventional source estimation or source-independent methods to CRG FWI. Therefore, in this study, we proposed inversion strategies for CRG FWI in both the time and frequency domains to deal with errors arising from different source wavelets between CRG traces. Then, we used a synthetic example for the Marmousi-II model and a real data example from the North Sea to demonstrate that our strategies for CRG FWI provide very similar inverted velocity models to those obtained from CSG FWI, at a lower computational cost.

全波形反演（FWI）是用于成像地下地质结构的最强大的地震数据处理技术之一，其计算成本与震源数量成正比。为了提高 FWI 的速度，我们探索了使用公共接收器道集 (CRG) 作为观察数据的普通炮集 (CSG) 的替代方案。这种方法有可能显着降低 FWI 的计算成本，特别是对于海底电缆 (OBC) 采集。当我们在基于 CSG 的 FWI 中匹配建模和观察到的 CSG 时，我们将观察到的 CRG 与基于 CRG 的 FWI 中切换源 - 接收器几何形状的建模 CSG 匹配。根据互惠原则，基于最速下降法或 Gauss-Newton 方法的 CRG FWI 产生与 CSG FWI 相同的反演速度模型，用于在整个源位置上应用相同且已知的源特征。然而，当源小波未知并且从一个源位置变化到另一个源位置时，CRG 的每条迹线都包含不同的源特征，这使得传统的源估计或与源无关的方法难以应用于 CRG FWI。因此，在本研究中，我们提出了 CRG FWI 在时域和频域上的反演策略，以处理 CRG 轨迹之间不同源小波产生的误差。然后，