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stream capture
Pliocene river capture and incision of the northern Altiplano: Machu Picchu, Peru
Stacked megafans of the Kalahari Basin as archives of paleogeography, river capture, and Cenozoic paleoclimate of southwestern Africa
Early onset and late acceleration of rapid exhumation in the Namche Barwa syntaxis, eastern Himalaya
40 Ar/ 39 Ar mica dating of late Cenozoic sediments in SE Tibet: implications for sediment recycling and drainage evolution
Alluvial fan shifts and stream captures driven by extensional tectonics in central Italy
Ongoing bedrock incision of the Fortymile River driven by Pliocene–Pleistocene Yukon River capture, eastern Alaska, USA, and Yukon, Canada
Karst piracy: A mechanism for integrating the Colorado River across the Kaibab uplift, Grand Canyon, Arizona, USA
Abandonment of Unaweep Canyon (1.4–0.8 Ma), western Colorado: Effects of stream capture and anomalously rapid Pleistocene river incision
Aftermath of a stream capture: Cactus Park lake spillover and the origin of East Creek, Uncompahgre Plateau, western Colorado
Drainage capture and discharge variations driven by glaciation in the Southern Alps, New Zealand
U-Pb zircon dating evidence for a Pleistocene Sarasvati River and capture of the Yamuna River
Pleistocene reversal of the Fraser River, British Columbia
Stream capture as driver of transient landscape evolution in a tectonically quiescent setting
Abstract Neogene drainage development in southeastern Idaho has been influenced by drainage capture, Basin and Range faulting, volcanism, and the Late Pleistocene Lake Bonneville overflow and Bonneville Flood. In Marsh Valley, the Middle to Late Pleistocene sedimentary sequence is dominated by alternating lacustrine/paludal and alluvial sediments, which have yielded new 40Ar/39Ar, amino acid racemization, and luminescence age estimates. The pattern of sedimentation through time indicates poor drainage integration of southern Marsh Valley through most of the last ca. 640 ka and suggests slow basin subsidence along Quaternary faults mapped on the basin edges. Marsh Valley initially incised into that valley fill sequence ca. 19 ka, shortly before the Bonneville Flood. Marsh Creek is a markedly underfit stream occupying a meandering, broad valley carved into the valley fill sequence. These geomorphic and sedimentologic patterns suggest non-catastrophic Lake Bonneville overflow before and after the Bonneville Flood. In Portneuf Valley, ca. 8.5–7.4 Ma basin fill and a bedrock pediment are perched 800 m above the modern valley floor. Major incision of basin fill and bedrock by the ancestral Portneuf drainage system occurred prior to the Middle to Late Pleistocene, when two cut-fill events resulted in accumulation of alluvial fan deposits extending ~10–60 m above the modern valley floor and basalt extending ~10 m below to 20 m above the modern valley floor. Final incision by Lake Bonneville overflow is evident but relatively minor in comparison to the cumulative downcutting. Overall, incision is attributed to isostatic subsidence of the eastern Snake River Plain, which served as base level for the Portneuf drainage system after passage of the Yellowstone hot spot in late Miocene time.