Crustal stress and fault strength in the Canterbury Plains, New Zealand

The M w = 7.1 Darfield (Canterbury) and M w = 6.2 Christchurch earthquakes and related aftershocks in Canterbury, New Zealand have revealed a major hazard in the Canterbury region in the form of the Greendale Fault and a number of associated faults. The strength of these apparently low slip-rate faults may affect the recurrence intervals of subsequent earthquakes. We use P- and S-wave picks from a dataset of aftershocks of the Darfield earthquake to estimate earthquake locations and focal mechanisms. We use S waveforms to determine shear-wave splitting (SWS) parameters and we estimate the azimuth of the axis of maximum horizontal compression ( S Hmax ) from inversions of focal mechanisms. Two 2D methods of clustering the focal mechanisms for stress inversion are used, one to estimate the regional stress field and another to investigate variations in S Hmax with distance from the Greendale Fault. A 3D method is also used to investigate variations in S Hmax with depth. The tectonic stress field is remarkably uniform and has an average maximum horizontal compressive stress orientation of S Hmax = 116 ± 18 ° , forming an angle with the average strike of the Greendale Fault of c. 25°. However, several S Hmax estimates along the Greendale Fault from the regional 2D clustering method are sub-parallel to the fault strike ( 93.6 ± 13.1 ° , 100.8 ± 11.5 ° and 100.8 ± 12.6 ° ), indicating that the fault may be frictionally weak, in an Andersonian sense. This variation occurs via an anti-clockwise rotation of S Hmax southwards across the Greendale Fault. SWS fast directions (ϕ) generally match nearby S Hmax , suggesting stress-aligned micro-cracks, but ϕ estimates at stations Cch3 and MQZ, which are near known and inferred faults, are sub-parallel to these faults and differ greatly from nearby stress orientations, indicating structure-dependent anisotropy. A lack of seismicity in the area prior to the Darfield earthquake precludes detailed analysis of time variations. However, there are two end member scenarios: if the pre-seismic stress orientation near the Greendale Fault was in the same direction as we have measured after the earthquake, then it was mis-oriented for rupture. Alternatively, if the stress rotated from the average regional orientation during the earthquake, then we can use the rotation to determine that an average of c. 40% of the pre-seismic differential stress on the Greendale Fault was released during the Darfield earthquake.