Long profiles of strath terraces in young tectonic settings frequently display upstream or downstream convergence, dome-or basin-like warping and/or faulting (Fig.
The rates of erosional downcutting of strath terraces changed between 0.02 to 2 mm /yr, increasing in the Late Pleistocene and Holocene in the western portion of the Outer Western Carpathians (OWC), when intensive erosion was restricted to neotectonically active elevations truncated by the Raba and Dunajec river valleys (Zuchiewicz, 1984, 1995, 1998; Wojcik, 1989; Olszak, 2008).
Zuchiewicz (1983, 1984, 1985, 1988, 1992, 1995), based on climato- and allostratigraphic subdivisions of Quaternary fluvial series in the Outer Carpathians, attempted to calculate the rates of erosional dissection of strath terraces in successive Pleistocene stages and to analyse different types of deformation of individual straths, distinguishing four "neotectonic phases": at the beginning of the Pleistocene, in the Early Pleistocene, at the Brunhes/Matuyama boundary (Interglacial II, Cromerian Complex), and in the Holsteinian ("Nowy Sacz Phase" of greatest intensity and extent).
The Weichselian and Holocene terraces are cut-and-fill landforms, the remaining ones represent strath terraces (Wojcik, 1989).
The upper, poorly dissected reach of the upper Jasiolka River valley reveals strath terraces from the Saalian-2, Weichselian and Holocene times (Zuchiewicz, 1988).
The above review points to differentiated neotectonic behaviour of faults displacing or warping strath terraces of Pleistocene age.
Short-term episodes of deep incision of strath terraces were associated with early interglacial phases.
In more strongly uplifted areas, in turn, the number of strath terraces increases, and climate cycles of short duration (up to 20 thousand years) may lead to shaping of several erosional steps.
a., disturbed longitudinal profiles of strath terraces (Starkel, 1972; Zuchiewicz, 1991, 1995b), incomplete sequences of alluvia (Starkel, 1985), convex-upward slope profiles in some regions (Starkel, 1972), young changes in the drainage pattern (Gerlach et al., 1985; Zuchiewicz, 1987; Laskowska-Wysoczanska, 1995), tilting of Upper Pleistocene lacustrine sediments (Koszarski and Koszarski, 1985), and some examples of young subsidence in intramontane (Baumgart-Kotarba, 1991-92, 1996, 1997) and Carpathian Foredeep basins (Starkel, 1972; Laskowska-Wysoczanska, 1995).
Longitudinal profiles of individual strath terraces frequently show divergence, convergence or tilting that can be indicative of young tectonic control (Zuchiewicz, 1987, 1991, 1995b; Henkiel et al., 1988; Wojcik, 1989; Kukulak, 1993).