The link between water infiltration, deformation mechanisms and strain localisation in the mid crust – an example from the Badcall shear zone, NW Scotland

The rheology and mechanisms of strain localisation in the middle and lower crust is yet to be fully constrained, but advances in analytical techniques mean we can revisit previously studied areas and build upon understanding already gained.

A strain profile across a Laxfordian-age (2300-1700 Ma) amphibolite-facies shear zone at Upper Badcall, NW Scotland, provides an excellent backdrop to investigate the hydration-strain-deformation mechanism relationship in the granulite-facies garnet-pyroxene quartzofeldspathic gneiss host rock and cross-cutting 25 m wide isotropic dolerite Scourie dyke. Both the granulite faces gneissic banding and mafic dyke are initially oriented at a high angle to the shear zone boundary. With increasing proximity to the shear zone centre the host rocks become progressively rotated, more deformed and hydrated. Increasing strain results in new foliation development, general grain size reduction and full or partial replacement of pre-existing pyroxene and hornblende by lower-temperature hornblende.

Tatham and Casey (2007) showed the 65 m wide shear zone has an estimated maximum shear strain of 15, which drops to ~7 towards the edge of the shear zone, and falls to < 1 at distances ≥ 40 m from the shear zone centre. We present data from four new transects, taken at 50-100 m intervals along the mafic dyke, which detail the change in deformation style and patterns of strain localisation and intensity. Localised anastomosing high strain zones envelop lenses of undeformed dolerite, with 65-70% of protolith undeformed in the dyke 350 and 230 m from shear zone centre. This decreases to 30 and 0% of undeformed protolith 100 m from and within the shear zone, respectively. Mylonite sensu stricto makes up 10% of dyke at distances ≥ 100 m from the shear zone, which increases to 70% within the shear zone, while the remaining dyke forms a weak fabric evidenced by the shape change of mafic grain aggregates.

Microstructural analyses show a switch in dominant deformation mechanisms from dynamic recrystallisation 350 m from the shear zone, to dissolution-precipitation creep inside the shear zone, identified by a change in crystallographic and shape preferred orientation, and distinct microstructural observations. An introduction of ~10 area % quartz and a loss of feldspar in the mafic dyke inside the shear zone accompanies this switch in dominant deformation mechanisms. We outline microstructural observations characteristic of dissolution-precipitation creep within the shear zone, and propose localised infiltration of quartz-rich fluid facilitates a switch from dislocation creep to pervasive dissolution-precipitation creep resulting in rheological weakening and local strain localisation. Our results suggest that strain localisation in the mid crust may be highly dependent on local fluid availability as fluid presence may trigger a switch in deformation mechanism and, with that, significant localised rheological weakening.

Tatham, D.J. and Casey, M., 2007. Inferences from shear zone geometry: an example from the Laxfordian shear zone at Upper Badcall, Lewisian Complex, NW Scotland. Geological Society, London, Special Publications, 272(1), pp.47-57.