Geoscience Reference
In-Depth Information
Table 2.2
(continued)
Shear
joints
4
7
9
Shear
joints
2
8
stage, where the minimum tectonic stress r
3
of NW-
SE to E-W trend generated formation of neotectonic
superimposed depressions generally elongated NE-SW
(see Fig.
2.23
). The compression was subvertical
(uplifting) and it is well expressed by the striations on
the tectonic slickenside at sites 6, 10, 12, and 13.
The most intense deformations can be referred to
the Pyrenean phase (end Eocene). Then, under the
conditions of strong pressure of almost N-S direction
(see sites 5, 13, and 4), a southward thrusting of the
Albanian Dinarides onto the Krasta-C ukali zone
occurred. After the Middle Jurassic, Late Cimmerian,
and after that, Laramian tectonic deformations affec-
ted the massif of limestones and dolomites. Recon-
structions in sites 13, 14, 15, 16, and 2 are a clear
evidence of this. The Laramian Phase is characterized
by a strong subhorizontal northwest-southeast trend-
ing minimum principal stress r
3
.
The Late Cimmerian Phase shows features, which
are very similar to the contemporary tectonic stress
field.
Pyrenean Phase the whole massif has been displaced
to the south, presumably with some rotation, both
most ancient phases posse an element of relativity in
reconstructed directions of their principal tectonic
stress axes.
2.3.1.5 Relations Between Karst Formation
and Concrete Tectonic Conditions
The first step for determination of tectonic factors,
influencing karst formation, is the analysis of the
principal stresses that have led to the now observed
structural ruptures in the discussed rock massif. The
karst formation has started most likely at the end of
the Eocene-Oligocene stage. By this time, the dis-
placements of the limestone massif to the south had
calmed down, and its intense uplifting started.
The detailed observations carried out in the sites of
reconstruction of the tectonic stress field have resulted
in some changes of the ideas concerning the fault
network of the area. On the one hand, the normal
faults are complicated by strike-slip displacements,
Taking
into
consideration
that
during
the
