Codex @codex  0

An iron oxide, $\alpha \text{-}\mathrm{F}{\mathrm{e}}_2{\mathrm{O}}_3$. It typically has weaker induced magnetic susceptibility than magnetite but can preserve stable remanent magnetization.

Inelastic neutron scattering resolves $E_i-E_f\ne 0$. Through conservation of energy, a peak at positive $\hslash \omega$ identifies an allowed excitation energy; through momentum conservation, its location in $\mathbf{Q}$ constrains the spatial variation of that excitation. A phonon is a quantum of lattice vibration; a magnon is a quantum of a spin wave. Their different couplings make energy transfer alone insufficient to identify which was created.

Bertram Neville Brockhouse's aluminium experiment rotated a large single crystal, scanning analyzer angle for neutron groups. His vanadium comparison exposed the elastic resolution. Later magnetite measurements used a magnetic field intensity test to identify magnons.^[ref]

Successive orientations sample different wave vectors; analyzer settings distinguish outgoing energies. This supplies points on a dispersion relation, rather than only an angular diffraction pattern. Finite resolution can merge neighboring excitations; background, multiple scattering and processes involving several phonons can complicate interpretation. A lattice model is a testable explanation of selected features, not a guarantee that every spectral peak has the same origin.

Iron ore is naturally occurring material from which iron can be extracted under the relevant technical and economic conditions. Important iron-bearing minerals include hematite, $\mathrm{F}{\mathrm{e}}_2{\mathrm{O}}_3$, and magnetite, $\mathrm{F}{\mathrm{e}}_3{\mathrm{O}}_4$. Real ore also contains other minerals, so its composition differs from that of a pure iron oxide.^[ref]

Using approximate atomic masses, pure hematite contains $2(55.85)/(2(55.85)+3(16.00))\approx 69.9\%$ iron by mass. This is a mineral-composition calculation, not the grade of every ore deposit. Beneficiation, transport and removal of oxygen and unwanted constituents all influence whether a deposit is a useful feed for iron extraction.

Magnetite is the iron oxide $\mathrm{F}{\mathrm{e}}_3{\mathrm{O}}_4$, commonly described as containing both iron(II) and iron(III) in an inverse-spinel structure. Its magnetic order is ferrimagnetic.

The unequal magnetic contributions of its sublattices leave a net magnetization. This makes magnetite a useful connection between oxidation-state chemistry, crystal structure, and bulk magnetism.

The main distinction is between metallic iron, iron(II) preparations, iron(III) preparations, and mixed iron oxides. The old prefixes “proto-” and “per-” ordinarily distinguish the lower and higher oxidation states here. “Peroxide of iron” means the historical iron(III) oxide preparation, not a modern peroxide containing an oxygen–oxygen bond.

The principal medicinal preparations can be grouped by the chemical form supplied:

These identifications follow the historical monographs, rather than the names of present commercial supplements.^[ref] A green iron(II) sulfate solution gives the characteristic blue reaction with potassium ferricyanide, whereas the higher iron solutions give blue with potassium ferrocyanide. Those diagnostic reactions explain why the official tests distinguish the two oxidation states; the historical colour test alone does not establish every detail of a complex preparation's composition.

At terminal speed, the downward excess weight is balanced by Stokes's law drag:The subtraction of the displaced water mass includes buoyancy. Hence the Stokes settling velocity isA density is needed but is not supplied. For the estimate, take a dense iron oxide represented by magnetite, with ${\rho }_p\simeq 5.2\times 10^3\mathrm{kg}{\mathrm{m}}^{-3}$, and water with ${\rho }_w\simeq 10^3\mathrm{kg}{\mathrm{m}}^{-3}$. This givesUsing the diameter for the particle Reynolds number gives $\mathrm{Re}\simeq {\rho }_w{v}_t(2a)/\eta \simeq 1.8\times 10^{-5}$, which supports the creeping-flow assumption. The model assumes a dilute isolated sphere far from walls and no imposed flow. The precise numerical speed depends on the unspecified oxide phase and particle density; the estimate is of order $10\mu \mathrm{m}{\mathrm{s}}^{-1}$.

Strong geological magnetic anomalies generally occur in rocks containing abundant strongly magnetic iron oxides, especially magnetite and titanomagnetite. Many mafic rocks, including basalt and gabbro, and some ultramafic rocks have large signatures; magnetite-rich iron formations can be exceptionally strong, while serpentinization can create additional magnetite. Actual magnetic susceptibility and remanent magnetization, rather than the rock name alone, determine the response. Sedimentary and felsic rocks are often weaker but have important exceptions.

Magnetite, titanomagnetite and maghemite exhibit strong ferrimagnetism; some pyrrhotite is also strongly magnetic. Hematite is generally much weaker in induced magnetic susceptibility, although it can carry stable remanent magnetization. Quartz and calcite have very small, usually negative, susceptibilities, and many ordinary silicates have only weak paramagnetism. A steel car exhibits strong ferromagnetism and can therefore stand out against a weakly magnetic host, but its shape and pre-existing remanent magnetization complicate the signal.^[ref]

Titanium-bearing iron-oxide solid solutions related to magnetite, commonly important carriers of magnetization in igneous rocks.