Erosion uplift rates

A General Concordance Between Erosion Rates and Uplift Rates... 

The globally S5mchronous development of erosion surfaces and slow uplift rates of shields indicates that models based on localized heating of the crust and mantle are not adequate to explain the uplift process. To produce near simultaneous surfaces on separate continents. King (1967) invoked global epeirogeny - uplift... 

The concentration of a stable cosmogenic nuclide in a sample that has experienced steady uplift during continuous exposure without erosion or burial requires integration over the range of elevations the sample experienced during exposure. For uplift rate u, modern elevation ymoderm and total exposure time T,... 

The existence of positive relief features and mountains is an almost self-explanatory indication that the rates of uplift of some continental sections have been much higher than the rates of denudation (Fig. 2). The rates of erosion that about balance or are slightly below the rates of uplift characterize the stable shield areas of South America, 10-20 mm ka and a tectonically active island Formosa (Taiwan), where uplift rates are as high as 103-104 mmka-1 (Stallard, 1988). 

In regions where land is steadily rising relative to mean sea level, the effects of sea-level fluctuations are sometimes recorded as ero-sional features on land. Whenever the rate of sea-level rise matches the rate of uplift, there is an apparent sea level still stand. Both deposition and erosion are controlled by this almost fixed base level, and a terrace may form. If sea level falls and again rises, the terrace will have risen sufficiently so that it is preserved upslope. Epi-... 

Snorre fault block is complex (Fig. 5). It includes an initial period of subsidence down to a depth of about 1500-1600 m until the Middle Jurassic (Bathonian-Callovian), followed by a period of uplift and erosion during the Late Jurassic and Early Cretaceous. The uplift culminated with a removal of 1200-1500 m of sediments, followed by a second period of subsidence with an onset in Valanginian-Hauterivian. A phase of very rapid subsidence took place during Late Cretaceous (Campanian-Maastrichtian), and another phase of high subsidence rate started in Pliocene-Pleistocene and is still going on. 

Figure 1. Linear rates (in millimeters per year) of chemical kinetic and macroscopic transport processes in surficial aquatic and sedimentary environments. Individual processes are coupled to the driving forces, identified as three main groups of chemical (C), hydrological (H), and physical (P) driving forces. Data sources mineral dissolution rates, Tables 4 and 5, and Berthelin (1988) mineral dehydration, compilation in Bodek and Lerman (1988) metal corrosion, Coburn (1968), Costa (1982), and Haynie and Upham(1970) uplift, Lajoie(1986), Stallard (1988) physical erosion, Table 3 chemical weathering, soil formation and chemical denudation, Table 6.

Physical denudation rates of 80-800 mm ka 1 would cause erosion of the land mass to the present-day mean elevation of continents, 840 m, in a period of 106-107 years if there were no crustal uplift compensating for, or exceeding, the rates of erosion. 

Tectonic processes provide the material of which landscapes are made. Tectonism produces uplift followed by erosion, or subsidence followed by deposition. Sediment storage makes the calculation of denudation rates rather time-scale-dependent. 

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