9 Denudation: Solute Transport and
Flux Rates of Terrigenous Sediment
9.1 Weathering, Soils, and F onnation of
Terrigenous Sediments
9.1.1 General Aspects
9.1.2 Modern Soils and Paleosols (Overview)
Introduction
Principal Soil Types
Soils Controlled by Sediment Aggradation or
Erosion
Cumulate, Composite, and Compound Paleosols
9.1.3 Weathering and Composition of Suspended
River Loads (Overview)
General Aspects and Problems
Minerals Derived from Parent Rocks
Climate Control ofSoil-Derived Minerals
Sediment Recycling
9.1.4 Detrital Clay Minerals in Lake Basins and
in the Sea
General Aspects
Paleoceanography and Paleoclimate from
Clay Minerals
9.2 Chemical Denudation (Quantitative Aspects)
9.2.1 Introduction
9.2.2 Groundwater Chemistry and Denudation Rates
in Specific Rock Types
Rock Salt and Sulfate Rocks
Carbonate Rocks
Silicate Rocks
9.2.3 Solute Transport ofRiver Systems
(Mixed Rock Types)
Solute Concentrations in Rivers
Global Mean Values ofSolute Concentrations
Variations in Water Chemistry Along
River Courses
9.2.4 Chemical Denudation Rates in Different
Morpho-Climatic Zones (Overview)
Specific Transport Rates and Mean
Denudation Rates (Definitions)
Examples from River Catchments and
Various Morpho-Clirnatic Zones
9.2.5 Global Effects ofChemical Denudation
9.2.6 Geomorphological Consequences of
Differential Chemical Denudation
9.3 Mechanical Denudation
9.3.1 Introduction
9.3.2 Modern Denudation Rates
The River-Load Method and Hs Limits
Mechanical Denudation Rates in Relation to
Relief and Climate
Results from Major River Systems
Results from Selected Regions and
Artificial Reservoirs
The Global Mechanical Denudation Rate
9.3.3 General Laws for Mechanical Denudation
9.4 Modern Chemical vs. Mechanical Denudation Rates
9.4.1 Global Values
9.4.2 Regional Variations and Trends
9.5 Long-Tenn Denudation Rates from Landfonn
Reconstruction
9.5.1 Methods for Reconstructing Fonner
Land Surfaces
9.5.2 Long-Tenn Denudation Rates (Overview)
9.5.3 Regions ofVery Slow Denudation
9.5.4 Modern vs. Long-tenn Denudation Rates
9.6 Steady State and Dynamic Denudation Systems
9.6.1 Isostatic Response to Denudation
9.6.2 Uplift and Denudation
General Concepts
Rates ofUplift
9.6.3 Simple Uplift-Denudation Models
9.7 Denudation Rates, Summary
9.1 Weathering, Solls, and Formation of
Terrigenous Sediments
9.1.1 General Aspects
Most of the sediment deposited in sedimentary basins
is derived from land areas exposed to subaerial
weathering. This is, to some extent, also true for
biogenic and chemical sediments, insofar as their
production depends on the dissolved river load delivered into the sedimentary basins. The land-derived,
solid material is usually referred to as the terrigenous, allochthonous, clastic component of a sedimentary deposit.
Due to weathering and erosion, the land surface is
slowly lowered (Fig. 9.1 a and b). The average
amount of this lowering in a certain region over a
given time span is defined as the mean denudation
rate. Denudation involves the transport of disintegrated bedrock, soil, and vegetation components into
continental basins or into the oceans. This mass
transfer is controlled by a variety of physical, chemical, and biological processes. Rainfall, surface runoff, and river flow are the most important transport
Flux Rates of Terrigenous Sediment
9.1 Weathering, Soils, and F onnation of
Terrigenous Sediments
9.1.1 General Aspects
9.1.2 Modern Soils and Paleosols (Overview)
Introduction
Principal Soil Types
Soils Controlled by Sediment Aggradation or
Erosion
Cumulate, Composite, and Compound Paleosols
9.1.3 Weathering and Composition of Suspended
River Loads (Overview)
General Aspects and Problems
Minerals Derived from Parent Rocks
Climate Control ofSoil-Derived Minerals
Sediment Recycling
9.1.4 Detrital Clay Minerals in Lake Basins and
in the Sea
General Aspects
Paleoceanography and Paleoclimate from
Clay Minerals
9.2 Chemical Denudation (Quantitative Aspects)
9.2.1 Introduction
9.2.2 Groundwater Chemistry and Denudation Rates
in Specific Rock Types
Rock Salt and Sulfate Rocks
Carbonate Rocks
Silicate Rocks
9.2.3 Solute Transport ofRiver Systems
(Mixed Rock Types)
Solute Concentrations in Rivers
Global Mean Values ofSolute Concentrations
Variations in Water Chemistry Along
River Courses
9.2.4 Chemical Denudation Rates in Different
Morpho-Climatic Zones (Overview)
Specific Transport Rates and Mean
Denudation Rates (Definitions)
Examples from River Catchments and
Various Morpho-Clirnatic Zones
9.2.5 Global Effects ofChemical Denudation
9.2.6 Geomorphological Consequences of
Differential Chemical Denudation
9.3 Mechanical Denudation
9.3.1 Introduction
9.3.2 Modern Denudation Rates
The River-Load Method and Hs Limits
Mechanical Denudation Rates in Relation to
Relief and Climate
Results from Major River Systems
Results from Selected Regions and
Artificial Reservoirs
The Global Mechanical Denudation Rate
9.3.3 General Laws for Mechanical Denudation
9.4 Modern Chemical vs. Mechanical Denudation Rates
9.4.1 Global Values
9.4.2 Regional Variations and Trends
9.5 Long-Tenn Denudation Rates from Landfonn
Reconstruction
9.5.1 Methods for Reconstructing Fonner
Land Surfaces
9.5.2 Long-Tenn Denudation Rates (Overview)
9.5.3 Regions ofVery Slow Denudation
9.5.4 Modern vs. Long-tenn Denudation Rates
9.6 Steady State and Dynamic Denudation Systems
9.6.1 Isostatic Response to Denudation
9.6.2 Uplift and Denudation
General Concepts
Rates ofUplift
9.6.3 Simple Uplift-Denudation Models
9.7 Denudation Rates, Summary
9.1 Weathering, Solls, and Formation of
Terrigenous Sediments
9.1.1 General Aspects
Most of the sediment deposited in sedimentary basins
is derived from land areas exposed to subaerial
weathering. This is, to some extent, also true for
biogenic and chemical sediments, insofar as their
production depends on the dissolved river load delivered into the sedimentary basins. The land-derived,
solid material is usually referred to as the terrigenous, allochthonous, clastic component of a sedimentary deposit.
Due to weathering and erosion, the land surface is
slowly lowered (Fig. 9.1 a and b). The average
amount of this lowering in a certain region over a
given time span is defined as the mean denudation
rate. Denudation involves the transport of disintegrated bedrock, soil, and vegetation components into
continental basins or into the oceans. This mass
transfer is controlled by a variety of physical, chemical, and biological processes. Rainfall, surface runoff, and river flow are the most important transport