The concept of hysteresis is fundamental when describing and comparing the magnetic properties of rocks. Hysteresis is the variation of magnetization with applied field and illustrates the ability of a material to retain its magnetization, even after an applied field is removed. Figure 9 illustrates this phenomenon in the form of a plot of magnetization (J) versus applied field (H_ex). J_s is the saturation (or “spontaneous”) magnetization when all the magnetic moments are aligned in their configuration of maximum order. It is temperature-dependent, reaching zero at the Curie temperature. J_r,sat is the remanent magnetization that remains when a saturating (large) applied field is removed, and J_r is the residual magnetization left by some process apart from IRM saturation, as, for example, TRM. H_c is the coercive field (or force) that is required to reduce J_r,sat to zero, and H_c,r is the field required to reduce J_r to zero.

Magnetic susceptibility is a parameter of considerable diagnostic and interpretational use in the study of rocks. This is true whether an investigation is being conducted in the laboratory or magnetic fields over a terrain are being studied to deduce the structure and lithologic character of buried rock bodies. Susceptibility for a rock type can vary widely, depending on magnetic mineralogy, grain size and shape, and the relative magnitude of remanent magnetization present, in addition to the induced magnetization from the Earth’s weak field. The latter is given as J_induced = kH_ex, where k is the (true) magnetic susceptibility and H_ex is the external (i.e., the Earth’s) magnetic field. If there is an additional remanent magnetization with its ratio (Q_n) to induced magnetization being given bythen the total magnetization iswhere k_app, the “apparent” magnetic susceptibility, is k(1 + Q_n).

Magnetic minerals and magnetic properties of rocks

The major rock-forming magnetic minerals are the following iron oxides: the titanomagnetite series, xFe₂TiO₄ · (1 - x)Fe₃O₄, where Fe₃O₄ is magnetite, the most magnetic mineral; the ilmenohematite series, yFeTiO₃ · (1 - y)Fe₂O₃, where α-Fe₂O₃ (in its rhombohedral structure) is hematite; maghemite, γ-Fe₂O₃ (in which some iron atoms are missing in the hematite structure); and limonite (hydrous iron oxides). They also include sulfides—namely, the pyrrhotite series, yFeS · (1 - y)Fe_{1 - x}S.

The Table gives some typical values of the apparent susceptibility for various rock types, which usually include some remanent as well as induced magnetization. Values are higher for mafic igneous rocks, especially as the content of magnetite increases.

A distribution of measured (true) susceptibilities for various rock types is shown in the Table. Basic refers to those rocks high in iron and magnesium silicates and magnetite, extrusive means formed by cooling after extruding onto the land surface or seafloor. The data in each category are based on at least 45 samples.

The Table lists representative values for the magnetic properties J_n (natural remanent magnetization), k (susceptibility), and ratio Q_n. Natural remanent magnetization is some combination of remanences; typically TRM in an igneous rock, perhaps DRM or CRM or both in a sedimentary rock, and all with an additional VRM. The ratio Q_n is typically higher for rocks with a strong, stable remanence—e.g., magnetite-rich and fine-grained extrusive rocks such as seafloor basalts.