7.2 Displacement along the ZSZ
To estimate the amount of ductile shearing that was accommodated by the ZSZ, we resorted to a simple trigonometric model which is presented in fig. 7.2.1. This model is based on the observation that, along a horizontal profile across the ZSZ, one can see the successive apparition of increasingly metamorphosed rocks, which equilibrated at very different depths, but are now at the same structural level. The net slip (s) required to bring two such rocks, initially separated by a vertical distance (DH), to the same structural level within a shear zone (dipping at an angle a) can easily be calculated by:
s = DH / sina. (1)
The equilibration depth of the various metamorphic zones is given either by thermobarometric results or by petrographic evidences and the present dip of the shear zone is known (20°). It is thus possible to calculate the net slip along the ZSZ.
(A) We consider the telescoping of the metamorphic zones to be essentially the result of simple shear. Pure shear is not considered in this model. Pervasive C/S fabrics within the ZSZ suggest, however, that extension occurred mainly through ductile simple shear.
(B) The topography during peak Barrovian metamorphism is assumed to be flat, the difference in equilibration depth would indeed be overestimated if the higher grade rocks equilibrated under a significantly higher topographic relief than the lower grade samples. A southward increasing topographic gradient is however very unlikely because of the observed gradual decrease in metamorphic conditions in the TH sediments forming the hanging wall of the ZSZ.
(C) The metamorphic field gradient observed across the ZSZ is here considered as representative of the thermal structure of the crust during metamorphism. This assumption is clearly false, because the metamorphic field gradient in any region is defined by a succession of mineral assemblages which equilibrated at peak temperature conditions but the peak temperatures were reached at different times for each metamorphic zone (fig. 7.2). The consequence is that the pressure at peak temperature is lower than immediately post-thrusting. However, as shown in figure 7.2 the difference in the depth of burial of two rocks (from two different metamorphic zones) directly after thrusting must be greater than when these same rocks have reached their respective maximal temperature. Hence, as we consider differences in equilibration depth for our calculation of the net slip, the consequence is that we under-evaluate this value.
The beauty of this trigonometric model however resides in its simplicity and in the fact that it is not influenced by the original angle formed between the metamorphic isograds and the shear zone.
The geothermobarometric data presented in chapter 5 indicate a maximal peak pressure difference of 320 ± 80 MPa between the samples from the garnet and the kyanite zone. Assuming a lithostatic pressure gradient of 27 MPa/km, this value can be converted into a vertical distance (DH) of 12 ± 3 km This value represent the finite vertical displacement to bring the lowermost kyanite zone sample to the same structural level as the uppermost garnet zone sample. Using this vertical distance DH ~12 ± 3 km and the present-day dip of the ZSZ a = 20°, a net displacement s = 35 ± 9 km is calculated with equation (1).
The net slip along the ZSZ in central Zanskar was estimated by Herren (1987) to be at least 25 km, on the basis of a geometrical model for the shearing of isograds. This model allows to calculate the net slip (s) along the shear zone using the equation:
s = (b / sinb)(h / h' - cosb) (2)
where h is the thickness of a supposedly unsheared rock sequence between two known isograds outside the ZSZ (measured in the western Suru area), h' is the thickness of the same sequence sheared within the ZSZ, b is the width of the ZSZ, and b is the dip of the ZSZ relative to the dip of the isograds outside the shear zone (b = 20°).
Equation (2) can be developed as:
s = (b*h / h'*sinb) - (b*cosa / sinb) (2.1)
s = (h*(b/h') / sinb) - (b / tanb) (2.2)
(2.2) is very similar to our own equation (1) because h*(b/h') is equivalent to DH and the term (b / tanb) only implies that one considers sampling perpendicular to the shear zone boundaries, instead of along a horizontal profile. The difference is anyway negligible. The major difference between the two equations is that Herren considers the angle b between the dip of the ZSZ and the dip of the isograds, where we only consider the dip of the shear zone (a)
Although this approach is broadly comparable to ours, it is based on some poorly constrained parameters. First, Herren (1987) measured a thickness h 6.3 km between the garnet to sillimanite isograds outside the ZSZ. This value appears surprisingly small compared to the DH = 12 ± 3 km of initial vertical distance between the garnet zone and kyanite zone samples, as indicated by our thermobarometry results. This difference suggests that, even outside the ZSZ, the isograds may have been thinned by the late- to post-metamorphic extensional structures scattered throughout the HHCS of Zanskar (Kündig, 1989). This process would lead to an underestimation of the original thickness of the sequence bound by known isograds, and therefore of the displacement along the ZSZ, using Herren's approach. In contrast, our estimate of the vertical displacement based on P-T results for peak conditions would not be affected. Secondly, Herren (1987) calculated the total thickness of the sequence before shearing as h ( b / h'). Because b and h' are both comparably small (0.35 and 0.25 km respectively in Herren, 1987), even small uncertainties in these two values have a major influence on the estimation of the total original thickness of the sequence now sheared within the ZSZ, and thus on the total movement. Thirdly, Herren's calculation of the net slip is dependant on the angle between the shear zone and the isograds which is difficult to estimate precisely.
Using the thermobarometric and the petrographic information to estimate the original thickness of the sheared metamorphic sequence proves to be much more accurate, as it allows to avoid most of the weakly constrained parameters used in Herren's purely geometrical model. Moreover our final calculation of the net slip along the ZSZ is independent of the original angle the isograds formed with the extensional structure.
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