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sinks
Jurassic tectonics of northeastern Gondwana: evidence from the detrital zircon record of the Nambour Basin
How did the world’s largest submarine fan in the Bay of Bengal grow and evolve at the subfan scale?
Ferrous hydroxychlorides hibbingite [γ-Fe 2 (OH) 3 Cl] and parahibbingite [β-Fe 2 (OH) 3 Cl] as a concealed sink of Cl and H 2 O in ultrabasic and granitic systems
Reconstructing source-to-sink systems from detrital zircon core and rim ages
Stratigraphy of late Quaternary mountain slope landforms and deposits in southern Africa and their significance for the dynamics of mountain sediment systems
Tracking Proterozoic–Triassic sediment routing to western Laurentia via bivariate non-negative matrix factorization of detrital provenance data
Super basin thinking: Methods to explore and revitalize the world’s greatest petroleum basins
Smamite, Ca 2 Sb(OH) 4 [H(AsO 4 ) 2 ]·6H 2 O, a new mineral and a possible sink for Sb during weathering of fahlore
Abiotic and Biotic Controls on Soil Organo–Mineral Interactions: Developing Model Structures to Analyze Why Soil Organic Matter Persists
ABSTRACT The Central Tertiary Basin (CTB) of Svalbard provides a rare opportunity for studying the sedimentary response to the Cenozoic evolution of the Barents Sea area. Here we present a basin model based on low-temperature thermochronology data, vitrinite reflectance measurements, and clay mineralogy from two drill cores inside the CTB. Our model suggests a tight relationship between the basin history and the regional geodynamic evolution. Enhanced heat flow during the Paleocene implies an extensional or transtensional origin of the basin, prior to Eurekan deformation. The first, compressional stage of the Eurekan orogeny was associated with rapid basin subsidence and high deposition rates, causing the coalification of the CTB hard coals. The second, transpressional stage of the Eurekan triggered rapid basin erosion and was associated with a decreasing heat flow. Onset of erosion is placed at ~45 ± 5 Ma, suggesting cessation of CTB deposition already by the late Early Eocene. Rapid erosion stopped coevally or just prior to the change to an extensional setting at the end of Eurekan deformation. Between ~40 and 10 Ma, the CTB experienced continuous slow erosion. From the Late Miocene onwards, erosion again accelerated, maybe related to lithospheric processes associated with northward propagation of the Knipovich Ridge. Estimates from our best-fit model suggest that nearly ~4 km of overburden was removed from the CTB since the end of Early Eocene.