3 - Magnetization Processes and Magnetic Properties of Sediments
Section snippets
Basic Principle
All matter responds to an applied magnetic field, due to the effect of the field on electron motions in atoms, although the response is very weak for most materials. The ions of some transitional metals, notably Fe2 +, Fe3 +, and Mn2 +, carry an intrinsic spin magnetic moment and are referred to as paramagnetic ions. Materials which contain these cations exhibit an enhanced response to an external field.
The weakest response is called diamagnetism. Diamagnetic materials do not contain paramagnetic
Magnetite (Fe3O4) and the Titanomagnetites (xFe2TiO4.[1 − x]Fe3O4)
Magnetite is one of the end members of the ulvospinel-magnetite solid solution series (Fig. 3.3) and is the most common magnetic mineral on Earth. Magnetite is a cubic mineral with inverse spinel structure. The disordering (Curie) temperature varies more or less linearly with Ti content from -150°C for ulvospinel to 580°C for magnetite (Fig. 3.4a). Hence, ulvospinel is paramagnetic at room temperature. Titanomagnetites are ferrimagnetic at room temperature for values of x below about 0.8.
Thermal Remanent Magnetization (TRM)
The remanent magnetization acquired by a grain during cooling through its blocking temperature is referred to as thermal remanent magnetization. The blocking temperature of a grain is the temperature above which the magnetic ordering in the grain is randomized by thermal energy during laboratory heating. The magnetic ordering of the grain will eventually become randomized at any temperature; the time that it is likely to take is referred to as the relaxation time (Tr), which is a function of
Magnetic Properties of Marine Sediments
The magnetic properties of marine sediments depend not only on the nature of primary magnetic minerals contributed from detrital or biogenic sources, or by precipitation from seawater, but also on the diagenetic conditions which determine the alteration of primary magnetic phases as well as the authigenic growth of secondary magnetic minerals. The important remanence-carrying minerals in marine sediments are magnetite (Fe3O4), titanomagnetite, hematite (α-Fe2O3), maghemite (γ-Fe2O3), geothite
Lake Sediments
In early studies of lake sediments, detrital hematite was considered to be the major carrier of remanence on the basis of the apparent observation of the Morin transition at – 10°C (Creer et al., 1972). Later studies showed that the reduction in magnetization intensity at this temperature was due to the reorientation of grains by growth of ice crystals and that the dominant carrier is fine-grained single domain magnetite (Stober and Thompson, 1977, Turner and Thompson, 1979). The grain size of
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