P. Schmoldt, PhD - MTNet - DIAS

A. Appendix
Anisotropy Resistivity
Misfit
RMS
r xx
Depth (km)
Depth (km)
100
150
200
250
300
0
rAA 50
Depth (km)
-1
0
1
2
3
4
TM
-1
0
1
2
3
4
Log 10(periods)-2
S N
0
50
100
150
200
250
300
0
ryy 50
TE
Log 10(periods)-2
100
150
200
250
300
synM11
synM11
synH10
0 30 60 90 120 150 180 210 240 270
Distance (km)
Apparent resistivity Log10(Wm) Phase
degrees
synG09
synF08
synE07
synD06
synC01
synH10
synG09
synF08
Log 10(Wm)
synE07
synD06
synM11
synH10
synG09
synF08
synE07
synD06
synC01
synC01
Total:
Log10(rxx)-Log10(ryy) Log10(Wm) Log10(Wm) 0.22
3.40
2.95
2.50
2.05
1.60
3.2
2.8
2.4
2.0
1.6
degrees
Fig. A.17.: Result of anisotropic 2D inversion for the 3D-crust-west profile with stations synM11 - synC01 on top of the synthetic 3D
model (cf. Figs. 8.3, 8.4, and 8.5 for synthetic 3D model, station location, and profile location). Station data is decomposed according
to the strike direction of the crust (N45W), and inversion is carried out with resistivity laplacian regularisation and an increased
smoothing parameter (τ = 6) following the first inversion approach: isotropic inversion of short-period data in the first sequence and
anisotropic inversion of long-period data in the second sequence. The less constrained location of the resistivity interface at upper
mantle depth in this model is attributed to smoothing constraints of the inversion and the large station spacing in the area.
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