s. The b.
to 20° N
axial pla-
al shorte-
tal levels
g.2, axial
tures are
antiform
Figure 2
1€
)ed under
tle-ductile
ne sucha
lateral off-
jart of the
the Ariab-
ne (KocH
al. 1983,
ear zones
| the area.
a sinistral
It can be
> accretion
gainst the
Good ex
amples occure E of Khor Langeb and along the Ema-
sa Shear Zone 80 km SSW of Sinkat the latter exhibi-
ting displacements of upto 5 km. Penecontemporane-
ously evolved structural elements include the brittle
displacement along the NW to NNW striking Oko she-
ar zone. The motion along this fault zone amounts to
6,5 km on a single displacement face (fig.3).
Figure 3: In this subscene the southern terminal of the Oko shear zone is displaye
migration path, and deformed the already exiting tec-
tonic patterns in the sheared complexes. This fact
allows to conclude that the shearing (Dg) predate
known ages of intrusions which took place in the late-
to postorogenic span of ca. 720 to 550 Ma (fig.2 upper
right) (KRONER 1985, ALMOND et al. 1989, KUSTER et
al. 1993).
^ Erkowit
Plain
3
d with its left-lateral
NW to NNW trending strike slip offset of approximately 6.5 km. Further explanation see text.
D; is a result of crustal thickening that gave rise to
anatexis at deeper levels and its emplacement as
diapiric bodies of often granitic to granodioritic compo-
sition into the upper crust. These intrusions heavily
relied on the previously developed steep faults as a
265
Dg is of particular interest because of its N-S directed
strike-slip faulting. Representing A-C-faults parallel to
the principal stress (0,). This deformation has sinistral
sense of movement and is differently displayed in the
whole area as seen on the processed images. Dis-
International Archives of Photogrammetry and Remote Sensing. Vol. XXXI, Part B7. Vienna 1996