In the evolutionary history of the Indian Peninsula extending for about 4 billion years, several episodic changes have taken place from time to time, leaving behind their imprints on the rocks and landscape. The drifting of shield segments, opening and closing of oceans, organic movements, development of mobile belts and extensive rifting are some of the important tectonic phases associated with Precambrian times. Vast areas of the Indian Shield comprised basement of Archean Crystallines represented by granite, gneiss and schistose rocks. Faulted basins and grabens were subsequently formed in the basement due to various tectonic processes during different times and were occupied by sediments belonging to Proterozoic, Palaeozoic, Mesozoic and Cenozoic ages. Extensive parts of Western and Central Peninsula were flooded with basaltic lava flows during late Cretaceous – early Tertiary period. Major tectonic activity subsided in Tertiary-Quaternary though minor movements continue to take place even in the present times. The breaking off of the Indian subcontinent from the Gondwana Mainland and its northward drift due to ocean floor spreading started in late Triassic period. In late Cretaceous, the subcontinent got detached from Madagascar and by early Eocene, separated from Sychelles. The free-drift of the subcontinent came to a halt during Eocene-Oligocene times with the commencement of subduction of its oceanic crust below the Tibetan plate. By about 45-40 My B.P., the neotethys ocean closed along the Indus-Tsang Posuture, and the cotlision of Indian and Tibetan continental crusts began thereby heralding the rise of the mighty Himalayas. Rifting in the Indian subcontinent along certain Precambrian structural trends started right since its detachment from the Mainland. In the western margin of the Indian Shield, the faulting was controlled by NE-SW Aravalli, ENE-WSW Son-Narmada-Tapti (SONATA) and NNW-SSE Dharwar trends (Biswas, 1982). Thus, during the migrating history of the subcontinent, three rifted basins, namely Kutch, Cambay and SONATA, developed (Figure 1). The SONA r A zone, traceable for a length of 1600 km, has been identified as a typical mid-continental rift, characterized by high gravity, positive isostasy, anomalous geothermal regime, shallowing of magnetic crust, elevated Curie point and moderate seismicity (Shanker, 1995). A large scale accreted igneous intrusion at the base of the crust beneath this zone has been postulated (Singh and Meissner, \995). Relative vertical movement upto one kilometer and lateral movement to the extent of 30 km have been established in the 150-200 km wide SONATA belt during Quaternary times (Shanker, 1987).