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  • The fluvial process of the lower Yellow River and its extension of river mouth deposits.
  • The old beds of the Yellow River can be found almost everywhere on the North China Plain. The cyclical process of the estuary development, namely, rerouting, extending, and rerouting again, is an epitome of the estuary development in the past
  • but on a big scale now. The extension of the river mouth is the direct cause of aggradation of the river bed above the point of estuary pivot, arising from large sediment load consequent to soil erosion in the upland areas. (TNC).
  • Processes of Holocene terrace formation in a steep gravel-bed river, Nikko volcanic area, central Japan
  • Flume experiments suggest that, in a breaded stream, terraces are formed from bars under erosional conditions. This paper examines these processes of terrace formation with the aid of field data on the Holocene terraces of the Nedori River
  • invasion is considered. According to the small scale cosmic photoes traces of numerous dry river beds-residues of the ancient river system are revealed, time stages of river beds migration and also it connection with aridisation phases and climate
  • The history of migration of now disappeared the Sarasvaty river and its tributaries in the Thar desert at the end of pleistocene-holocen and connected with the changes of the environment, the degree of watering landscapes, the character of land
  • Three major depositional systems were differentiated. The lower systems was characterized by relatively small fluvial systems. The following thick sandstone beds represent large fluvial channel complexes formed by a large sandy braided river, a thin
  • -bedded succession represents an abandonment of this system and a migration of the paleo-Indus towards the east to its present position. Finally, a system is formed by terminal fluvial fans, of which its modern analogue can be found within the intramontane
  • Through investigating 11 profiles of the bar, two types of vertical depositional sections are recognized, one dominated by large trough cross-bedding and the other by opposite inclined bedding. The point bar is divided into six sub-facies according
  • to the geomorphological location, texture and structure of the deposits. The origin of the two kinds of intersecting bedding is discussed. (TNC).
  • was about 500 mm/yr, or about 200 mm/yr above the modern value. After about 3,500 yr B.P., the Lunkaransar profile indicated a desiccated lake bed.
  • faults near maximum sediment thickness. These faults, indicative of regional tension, played a dominant role in the basins'evolution. The terrestrial clastics and coal beds in the Damodar-Son and Satpura basins are cut by ultrabasic and basic dykes