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The integrated approach combining kinematic and structuralparagenetic field tectonophysics techniques allows us to construct a continuous time scan of the stressstrain state (SSS) and deformation modes (DM) from sediment lithification to the final orogenic process for the studied areas. Definitions of the continuous sequence of SSS and DM provide for control of the known geodynamic reconstructions and adjustment of geodynamic models. An example is the tectonophysical study of the Alpine structural stage of the Western Mountainous Crimea (WMC) and the PreCambrian complexes of the Ukrainian Shield (USh). Data from WMC allow us to make adjustments to the geodynamic model of the Mountainous Crimea. In particular, tra jectories of the principal normal stresses (Fig. 4 and 5), both for shifts and shear faults with reverse components/ normal faults, suggest the reverse nature of movements of the Eastern and Western Black Sea microplates with their overall pushing onto the Crimean peninsula in the southeast, south and southwest (Fig. 7). In the Precambrian USh complexes (Fig. 8), 13 stages of regional deformation are revealed between ≥2.7 and 1.6 billion years ago. Until the turn of 2.05-2.10 billion years, the region was subject to transtension and transpression, as the Western (gneissgranulite) and Eastern (granitegreenstone) Archean microplates of USh moved to separate from each other in the NeoArchean and then diverged and converged in the Paleoproterozoic (movements at a sharp angle). It is assumed that in the Archean the Western and Eastern microplates were separated by the oceanic or suboceanic lithosphere (Fig. 12, 13). During the period of 2.3-2.4 billion years, the plates fully converged creating a zone of collision. It may be suggested that a possible mechanism for the oceanic window closeup was underthrusting of the upper suboceanic lithosphere layers beneath the crustmantle plates on gently sloping breakup surfaces (nonsubduction option), and one of them is Moho. Spreading of the Western and Eastern microplates of USh began at the turn of 2.05-2.10 billion years, as evidenced by the available tectonophysical data on fields of latitudinal extension of the crust. During spreading 2.1-2.05 billion years ago, emanations and solutions were able to ascend into the upper crust and thus stimulate palingenesis (Novoukrainsky and Kiro vogradsky granites), and during repeated spreading 1.75 billion years ago, magma of the basic and acid composition (Pluto gabbroanorthosite and rapakivi) intruded into the upper crust. The spreading zone coincided with the former collisional su ture and became the site wherein the interregional KhersonSmolensk suture was formed; it stretches submeridionally across the East European platform.

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Precambrian granulites of the Aldan shield in southern Yakutia, USSR, form a massif of 200,000 km' bounded by younger fold-belts to the south, west and east. The massif consists of several blocks that reflect a primary heterogeneity of composition and differences in structural and thermodynamic evolution ofdifferent parts of the area. According to structural and petrological data the massif can be divided into two megablocks: eastern Aldan and western Aldan. They are separated by a narrow meridional fold-belt. Structural evolution of this central zone was determined by the geodynamics of the megablocks and was completed in the late Archaean. Towards the south, this central zone is 'transformed' into the relatively small Sutam block adjoining the Stanovoy fold-belt that bounds the Aldan shield on the south. The Sutam block is separated from t.he other structural units of the Aldan shield by a system of north trending grabens filled by post-Archaean sediments.The Aldan shield is composed of Archaean high-grade granulites, while the Stanovoy foldbelt, to the south, consists of highly foliated Proterozoic rocks metamorphosed under relatively lower-grade conditions. However, relics of the granulites are mapped within the fold-belt.