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