1. Weathering Types: Physical or mechanical (increases surface area) Chemical (chemical transformations) –Congruent (complete dissolution) –Incongruent (solids + dissolved products)

2. Factors Controlling Chemical Weathering Rates Mineralogy Surface area pH Temperature Organic acids Rate = d(mineral mass)/dt = -KA Where A = surface area and K=parameter reflecting all other controls

3. Effect of Mineral Type In general, rate decreases with: 1. Increasing tetrahedral linkages 2. Less Al for Si. Faster than olivine Slower than olivine

4. Measuring Weathering Rates 1. Streams Instantaneous measures Integrates area 2. Soils Integrates time Site specific

5. EBMUD Water Chemistry and Mineral Weathering

6. Sierran Spring Chemistry and EBMUD Water Lafayette2.4 1.1 0.4 0.13 2.8 Orinda3.3 1.8 0.6 0.15 5.4

7. Typical Weathering Reactions Reaction medium consists of water and CO 2 Products kaolinite and gibbsite plus dissolved products

8. Sierran Spring Chemistry and EBMUD Water Lafayette2.4 1.1 0.4 0.13 2.8 Orinda3.3 1.8 0.6 0.15 5.4 Subtract contribution from rain (i.e. assume all Cl and SO4 from rain - balanced by Na) Assume all Mg derived from biotite.15(B)+.15(H2CO3)+.15(.5H20)=.15(K)+.15(3Mg)+.15(7HCO3)+.15(2H4SiO4)+.15(.5 Kaol) Assume all K from K spar

9. Chemical vs. Mechanical Weathering: Role of Climate and Geology Recently glaciated, tectonically active areas have high chemical weathering rates Areas of long term stability (and long weathering history have lower rates (Aust, Africa) Chemical weathering an important means of denudation

10. Soil Based View of Weathering: Chemical Mass Balance (Brimhall and others) Give soil profile based perspectives –Depth variations –Climate variations –Age variations Gives us view of both physical and chemical changes in soils during development –Soils commonly undergoe initial expansion followed by collapse –Soils, given enough time, can become chemically depleted and must rely on atmospheric inputs