What is Mössbauer Spectroscopy
Fundamental Principles of Mössbauer Spectroscopy
Eγ-ray emission = Etransition - ER,
Eγ-ray emission = the energy of the emitted γ-ray
Etransition = the energy of the nuclear transition
ER = the energy of the recoil.
The Mössbauer effect occurs because in solids, the value of f is high enough that recoil-free absorption is possible. Thus an atom of 57Co can decay to 57Fe, which gives off a γ-ray, and may be absorbed without recoil by a nearby 57Fe, which happens to have just the right splitting between the energy levels in its nucleus to absorb it. This scenario will only happen if the decaying Co atom is surrounded by the same atoms as the absorbing Fe. If the receiving Fe atoms are in a different matrix (say, in a mineral) than in the emitter, then no absorption can occur.
So Mössbauer spectra are described using three parameters: isomer shift (δ), which arises from the difference in s electron density between the source and the absorber, quadrupole splitting (Δ which is a shift in nuclear energy levels that is induced by an electric field gradient caused by nearby electrons, and hyperfine splitting (for magnetic materials only). Graphically, quadrupole splitting is the separation between the two component peaks of a doublet, and isomer shift is the difference between the midpoint of the doublet and zero on the velocity scale (Figure 3). Mössbauer parameters are temperature-sensitive, and this characteristic is sometimes exploited by using lower temperatures to improve peak resolution and induce interesting magnetic phenomena.
If the electrons around the Fe atom create a magnetic field, as in the case of magnetite, then the energy levels in the Fe nucleus will split to allow six possible nuclear transitions, and a sextet (six-peak) spectrum results. The positions of the peaks in the sextet defines what is called the hyperfine splitting (Hint or BHf, depending on the units used) of the nuclear energy levels.
Iron atoms in different local environments and those having different oxidation states absorb at different, diagnostic energies. A typical Mössbauer spectrum thus consists of sets of peaks (usually doublets and sextets), with each set corresponding to an iron nucleus in a specific environment in the sample (an Fe nuclear site). Different sets of peaks appear depending on what the Fe nucleus "sees" in its environment. The nuclear environment depends on a number of factors including the number of electrons (Fe0, Fe2+, Fe3+), the number of coordinating anions, the symmetry of the site, and the presence/absence of magnetic ordering (which may be temperature-dependent). Thus the spectrum of a given mineral may consist of a superposition of doublets and sextets.
As seen in Figure 4, Fe atoms in minerals are predictably found in coordination polyhedra of appropriate size based on radius ratios. The top half of Figure 4 plots the isomer shift and quadrupole splitting of several minerals whose iron valence state and coordination number are independently known (usually from single crystal X-ray diffraction), and the bottom of the figure shows the resultant groupings. Fe3+ occurs primarily in 4- or 6-coordination with oxygen, while Fe2+ may be rarely 4- or 5- coordinated, commonly 6-coordinated, and occasionally 8-coordinated with oxygen. Fe in 4-fold coordination with sulfur has subtly different parameters due to the effects of covalent bonding. Variations in Mössbauer parameters that are characteristic of each type of coordination polyhedron can be related to polyhedral site distortion; a thoughtful discussion of this topic can be found in Burns & Solberg (1988).
Mössbauer Spectroscopy Instrumentation - How Does It Work?
In some cases, Mössbauer spectrometers are also used to identify minerals. This application is limited, however, by the fact that many different minerals can have site geometries that are the same, such that their Mössbauer spectra and the resultant peak parameters will also be the same. For example, the spectra of amphibole and pyroxene group minerals are all very similar, so you could not tell these minerals apart by their Mössbauer spectra alone!
Strengths and Limitations of Mössbauer Spectroscopy?
The vast majority of rock-forming minerals on Earth contain Fe2+ in octahedral coordination, and thus have very similar Mössbauer parameters. For example, pyroxene, amphibole, and mica spectra are all nearly indistinguishable. Furthermore, most minerals exhibit a range of Mössbauer parameters as a function of cation substitution. Finally, the parameters vary as a function of temperature, and the magnitude of that variation is distinctive to each mineral composition. For these reasons, Mössbauer spectroscopy is not ideally suited to mineral identification (except for iron oxides, where magnetic properties can be extremely diagnostic) and is typically not used for this purpose (though it has been pressed into such service in extraterrestrial applications).
User's Guide - Sample Collection and Preparation
In most laboratories, samples are mixed with some inert material such as sucrose of graphite to assist in spreading the sample evenly across the diameter of the sample holder. The sample is them held in place with something thin and non-absorbant to γ-rays such as cellophane or kapton tape.
Data Collection, Results and Presentation
Software for analysis of Mössbauer spectra uses a variety of different physical models to generate model spectra with which to compare the measured spectra, and different fitting algorithms to analyze the data. It is important to assume a theoretically reasonable model when fitting Mössbauer spectra because it is possible, based on the data alone, to fit spectra to an unphysical model and still get superficially reasonable chi-squared values. Three different line shapes are commonly employed in modeling of Mössbauer spectra (Figure 6).
- Lorentzian (Cauchy) line shapes, used to describe spectral lines resulting from broadened resonance and other phenomena, have been used since the technique was first developed. This line shape gives a good approximation of line shapes in spectra of paramagnetic materials where all of the Fe nuclei are in identical electronic environments. It is less useful when variations in the geometry of the coordination polyhedra and variable distance between the Fe atom and nearest oxygens and next nearest cations occur—as is the case in most minerals.
- Beginning in the 1970's, many Mössbauer routines began to address the variations in coordination polyhedra around the Fe nucleus by adding a Gaussian component to the Lorentzian line shape. The resultant hybrid line shape, which is a Gaussian distribution of Lorentzian line shapes, is called a Voigt line shape, and is generally approximated by a linear combination of the two line shapes that is called a pseudo-Voigt function (Figure 6).
- Quadrupole splitting distributions (QSDs) are a further evolution in modeling Mossbauer spectra of minerals in which there are poorly-resolved quadrupole pairs, as is certainly the case in phyllosilicate spectra. The QSDs model the local distortions and atomic disorder surrounding the Fe atoms, rather than simply reflecting the ideal point symmetries of the relevant sites. The QSD method performs better than Lorentzian fits in a number of ways. Fits with Lorentzian doublets tend to overestimate the spectral backgrounds, put large wings or tails on the main absorption peaks, and give unreasonably large linewidths.
One final and fundamental constraint on geological applications of Mössbauer results must be mentioned because it is frequently misunderstood. 57Fe Mössbauer spectroscopy can determine only the relative amounts of iron in various types of sites and valence states. It cannot determine the total number of Fe atoms that are present in a material (i.e., relative to the other atoms present) because the presence of other elements has no effect on the Mössbauer spectrum except as they alter the Fe environment and reduce the overall intensity of the spectrum, but not its dependence on velocity. It should be emphasized, therefore, that Mössbauer spectroscopy is a tool to investigate the nature and relative contents of Fe-bearing minerals in a sample. It provides no information on minerals that do not contain Fe in their structures.
The following literature can be used to further explore Mössbauer Spectroscopy
- Bancroft, G.M. 1973. Mössbauer spectroscopy: an introduction for inorganic chemists and geochemists. Wiley and Sons, New York, 251 pp.
- Burns, R.G., and Solberg, T.C. 1988. 57Fe-bearing oxide, silicate, and aluminosilicate minerals. In Spectroscopic Characterization of Minerals and Their Surfaces, L.M. Coyne, D.F. Blake, and S.W.S. McKeever, Eds. American Chemical Society Symposium, Series, pp. 263-282. Oxford: Oxford University Press.
- DeGrave E, Vandenberghe RE, Dauwe C. 2005. ILEEMS: Methodology and applications to iron oxides. Hyperfine Interactions, 161 (1-4): 147-160.
- Dyar, M.D. Agresti, D.G., Schaefer, M., Grant, C.A., and Sklute, E.C. 2006. Mössbauer spectroscopy of earth and planetary materials. Annual Reviews of Earth and Planetary Science, 34, 83-125.
- Hawthorne, F.C. 1988. Mössbauer spectroscopy. Reviews in Mineralogy, 18, 255-340.
- May L, editor. 1971. An introduction to Mössbauer spectroscopy. New York: Plenum. 203 pp.
- McCammon, C.A. 1994. A Mössbauer milliprobe: Practical considerations. Hyperfine Interactions, 92, 1235-9.
For more information about Mössbauer Spectroscopy follow the links below.
- The Mössbauer Effect Data Center ( This site may be offline. ) provides information resources to Mössbauer researchers around the world, including databases, handbooks, searches, conference postings, and other useful information.
- This site gives educational information about Mössbauer spectroscopy, and background on how the technique is being used on Mars. Its database contains over 3,000 Mössbauer spectra of rock-forming minerals acquired at temperatures from 4-300K.
Other Resources on Mineral Spectroscopy
Teaching Activities and Resources
Teaching activities, labs, and resources pertaining to Mössbauer Spectroscopy.