Electron microprobe

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A Cambridge Scientific Instrument Company "Microscan" electron probe microanalyzer based on a design by David Wittry. This model is housed at the Cambridge Museum of Technology

An electron microprobe (EMP), also known as an electron probe microanalyzer (EPMA) or electron micro probe analyzer (EMPA), is an analytical tool used to non-destructively determine the chemical composition of small volumes of solid materials. It works similarly to a scanning electron microscope: the sample is bombarded with an electron beam, emitting x-rays at wavelengths characteristic to the elements being analyzed. This enables the abundances of elements present within small sample volumes (typically 10-30 cubic micrometers or less) to be determined.[1] The concentrations of elements from boron to plutonium can be measured at levels as low as 100 parts per million (ppm). Recent models of EMPAs can accurately measure elemental concentrations of approximately 10 ppm.

History[edit]

Development of the electron microprobe was preceded by that of the closely related analytical technique of X-ray fluorescence spectrometry (XRF). This technique was first proposed by Georg von Hevesy in 1923 and applied by other workers in the following few years.

In 1944, MIT built an electron microprobe, combining an electron microscope and an energy-loss spectrometer. Electron energy-loss spectrometry is very good for light element analysis and they obtained spectra of C-Kα, N-Kα and O-Kα radiation. In 1947, Hiller patented the idea of using an electron beam to produce analytical X-rays, but never constructed a working model. His design proposed using Bragg diffraction from a flat crystal to select specific X-ray wavelengths and a photographic plate as a detector.

In 1948-1950, Raymond Castaing, supervised by André Guinier, built the first electron “microsonde électronique” (electron microprobe) at ONERA. This microprobe produced an electron beam diameter of 1-3 μm with a beam current of ~10 nanoamperes (nA) and used a Geiger counter to detect the X-rays produced from the sample. However, the Geiger counter could not distinguish X-rays produced from specific elements and in 1950, Castaing added a quartz crystal between the sample and the detector to permit wavelength discrimination. He also added an optical microscope to view the point of beam impact. The resulting microprobe was described in Castaing's 1951 PhD Thesis,[2] in which he laid the foundations of the theory and application of quantitative analysis by electron microprobe, establishing the theoretical framework for the matrix corrections of absorption and fluorescence effects. Castaing (1921-1999) is considered the "father" of electron microprobe analysis.

Cameca (France) produced the first commercial microprobe, the “MS85,” in 1956. It was soon followed by many microprobes from other companies; however, all companies except Cameca and JEOL, are now out of business. In addition, many researchers build electron microprobes in their labs. Significant subsequent improvements and modifications to microprobes included scanning the electron beam to make X-ray maps (1960), the addition of solid state EDS detectors (1968) and the development of synthetic multilayer diffracting crystals for analysis of light elements (1984).

How it works[edit]

A beam of electrons is fired at a sample. The beam causes each element in the sample to emit X-rays at a characteristic frequency; the X-rays can then be detected by the electron microprobe.[3] The size and current density of the electron beam determines the trade-off between resolution and scan time and/or analysis time.[4]

Detailed description[edit]

Low-energy electrons are produced from a tungsten filament, a lanthanum hexaboride crystal cathode or a field emission electron source and accelerated by a positively biased anode plate to 3 to 30 thousand electron volts (keV). The anode plate has central aperture and electrons that pass through it are collimated and focused by a series of magnetic lenses and apertures. The resulting electron beam (approximately from 5 nm to 10 micrometre diameter) may be rastered across the sample or used in spot mode to produce excitation of various effects in the sample. Among these effects are: phonon excitation (heat), cathodoluminescence (visible light fluorescence), continuum X-ray radiation (bremsstrahlung), characteristic X-ray radiation, secondary electrons (plasmon production), backscattered electron production, and Auger electron production.

When the beam electrons (and scattered electrons from the sample) interact with bound electrons in the innermost electron shells of the atoms of the various elements in the sample, they can scatter the bound electrons from the electron shell producing a vacancy in that shell (ionization of the atom). This vacancy is unstable and must be filled by an electron from either a higher energy bound shell in the atom (producing another vacancy which is in turn filled by electrons from yet higher energy bound shells) or by unbound electrons of low energy. The difference in binding energy between the electron shell in which the vacancy was produced and the shell from which the electron comes to fill the vacancy is emitted as a photon. The energy of the photon is in the X-ray region of the electromagnetic spectrum. As the electron structure of each element is unique, the series X-ray line energies produced by vacancies in the innermost shells is characteristic of that element, although lines from different elements may overlap. As the innermost shells are involved, the X-ray line energies are generally not affected by chemical effects produced by bonding between elements in compounds except in low atomic number (Z) elements ( B, C, N, O and F for Kalpha and Al to Cl for Kbeta) where line energies may be shifted as a result of the involvement of the electron shell from which vacancies are filled in chemical bonding.

The characteristic X-rays are used for chemical analysis. Specific X-ray wavelengths or energies are selected and counted, either by wavelength dispersive X-ray spectroscopy (WDS) or energy dispersive X-ray spectroscopy (EDS). WDS utilizes Bragg diffraction from crystals to select X-ray wavelengths of interest and direct them to gas-flow or sealed proportional detectors. In contrast, EDS uses a solid state semiconductor detector to accumulate X-rays of all wavelengths produced from the sample. While EDS yields more information and typically requires a much shorter counting time, WDS is generally a more precise technique with lower limits of detection because its superior X-ray peak resolution.

Chemical composition is determined by comparing the intensities of characteristic X-rays from the sample material with intensities from known composition (standards). Counts from the sample must be corrected for matrix effects (depth of production of the X-rays,[5][6]absorption and secondary fluorescence[7][8]) to yield quantitative chemical compositions. The resulting chemical information is gathered in textural context. Variations in chemical composition within a material (zoning), such as a mineral grain or metal, can be readily determined.

Volume from which chemical information is gathered (volume of X-rays generation) is 0.3 – 3 cubic micrometers.

Uses[edit]

Materials science and engineering[edit]

A section of the 1886VE10 microcontroller die as seen by an electron microprobe. The small bright cylinders are tungsten vias left over from a metalization etching process. The X-ray spectroscopy technique can be used to determine the material composition of the vias.
For comparison purposes, a similar section of the 1886VE10 microcontroller die as seen by an optical microscope.

The technique is commonly used for analyzing the chemical composition of metals, alloys, ceramics, and glasses. It is particularly useful for assessing the composition of individual particles or grains and chemical changes on the scale of a few micrometres to millimeters. The electron microprobe is widely used for research, quality control, and failure analysis.

Mineralogy and Petrology[edit]

This technique is most commonly used by mineralogists and petrologists. Most rocks are aggregates of small mineral grains. These grains may preserve chemical information adopted during their formation and subsequent alteration. This information may illuminate geologic processes, such as crystallization, lithification, volcanism, metamorphism, orogenic events (mountain building), plate tectonics. This technique is also used for the study of extraterrestrial rocks (i.e. meteorites), and provides chemical data which is vital to understanding the evolution of the planets, asteroids, and comets.

The change in elemental composition from the center (also known as core) to the edge (or rim) of a mineral can yield information about the history of the crystal's formation, including the temperature, pressure, and chemistry of the surrounding medium. Quartz crystals, for example, incorporate a small, but measurable amount of titanium into their structure as a function of temperature, pressure, and the amount of titanium available in their environment. Changes in these parameters are recorded by titanium as the crystal grows.

Palaeontology[edit]

In exceptionally preserved fossils, such as those of the Burgess shale, soft parts of organisms may be preserved. Since these fossils are often compressed into a 2D film, it can be difficult to deduce what features were what: a famous example is that of triangular extensions in Opabinia, which were interpreted as either legs or extensions of the gut. Elemental mapping showed that they had a similar composition to the gut, favouring the second interpretation.[9] Because of the thin nature of the carbon films, only low voltages (5-15 kV) can be used in such specimens.[10]

For more information about element abundance in the Burgess shale, see Burgess shale type preservation#elemental mapping

Meteorite Analysis[edit]

The chemical composition of meteorites can be analysed quite accurately using EPMA technique. This can reveal a lot of information about the conditions that existed in our Solar System many years ago. Thus, in helping us know the past of our Solar System, it will also put us a step ahead in knowing the present & maybe, even future conditions of Solar System.

See also[edit]

References[edit]

  1. ^ Wittry, David B. (1958). "Electron Probe Microanalyzer", US Patent No 2916621, Washington, DC: U.S. Patent and Trademark Office.
  2. ^ Castaing, Raimond (1952) [Submitted 1951]. Application des sondes électroniques à une méthode d'analyse ponctuelle chimique et cristallographique: publication ONERA (Office national d'études et de recherches aéronautiques/ Institute for Aeronautical Research) N. 55 (PhD Thesis). University of Paris. 
  3. ^ Jansen, W.; Slaughter, M. (1982). "Elemental mapping of minerals by electron microprobe" (PDF). American Mineralogist 67 (5–6): 521–533. 
  4. ^ http://serc.carleton.edu/research_education/geochemsheets/elementmapping.html
  5. ^ Duncumb P. and Reed S.J.B., NBS Spec. Publ. 298, Heinrich K.F.J. ed., 1968, p. 133
  6. ^ Bishop H.E., 4th Int. Congr. X-Ray Opt., Orsay, Hermann, Paris, 1966, p. 153
  7. ^ S.J.B. Reed, Electron microprobe analysis, Cambridge University Press, 1993
  8. ^ K.F.J. Heinrich, and D.E. Newbury eds., Electron probe quantitation, Plenum Press, 1991
  9. ^ Zhang, X. & Briggs, D.E.G. (2007). "The nature and significance of the appendages of Opabinia from the Middle Cambrian Burgess Shale". Lethaia 40 (2): 161–173. doi:10.1111/j.1502-3931.2007.00013.x. Retrieved 2008-08-20. 
  10. ^ Orr, P. J.; Kearns, S. L.; Briggs, D. E. G. (2009). "Elemental mapping of exceptionally preserved ‘carbonaceous compression’ fossils". Palaeogeography Palaeoclimatology Palaeoecology 277 (1–2): 1–8. doi:10.1016/j.palaeo.2009.02.009.  edit

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