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Secondary Ion Mass Spectrometer (SIMS)

Paul Mueller, University of Florida
Jeff Vervoort, Washington State University

What is Secondary Ion Mass Spectrometer (SIMS)

As a class, SIMS instruments (aka ion microprobes) use an internally generated beam of either positive (e.g., Cs) or negative (e.g., O) ions (primary beam) focused on a sample surface to generate ions that are then transferred into a mass spectrometer across a high electrostatic potential, and are referred to as secondary ions. In a similar technique, a beam of high-speed neutral atoms (e.g., Ar) can substitute for the primary ion beam, an approach used primarily for surface analysis of organic compounds that has few applications in the geosciences and is not discussed here.

Fundamental Principles of Secondary Ion Mass Spectrometer (SIMS)

Schematic depiction of SIMS source region. Details

The interaction of the primary ion beam with the sample (under vacuum) provides sufficient energy to ionize many elements. If the primary beam is composed of positively charged ions, the resultant ionization favors production of negative ions; primary beams of negative ions favor generation of positive ions. Although most atoms and molecules removed from the sample by the interaction of the primary beam and the sample surface (referred to as sputtering) are neutral, a percentage of these are ionized. These ions are then accelerated, focused, and analyzed by a mass spectrometer.

In "dynamic SIMS" mode the primary ion beam exceeds the "static limit" (~1E12 ions/cm2) producing a high yield of secondary ions. This technique is used for "bulk" analysis of elements and isotopes, and is particularly well-suited for analysis of isotopes and trace elements in minerals (e.g. REE in garnet). Alternatively, "static SIMS" uses a much lower energy primary ion beam (usually Ga or Cs). This technique is typically used for analysis of atomic monolayers on material surfaces to obtain information about molecular species on material surfaces (e.g. organic compounds; see module on Time-of-Flight SIMS.

Secondary Ion Mass Spectrometer (SIMS) Instrumentation - How Does It Work?

Typical forward geometry SIMS/ion microprobe configuration (Cameca IM 6f) showing: 1) negative primary beam source, 2) positive primary beam source, 3) electrostatic lens for primary beam, 4) sample stage and sputtering, 5) electrostatic sector, 6) magnetic sector, 7) collectors, and 8) ion imaging detector. Click image to enlarge. Details
There are several different designs of SIMS currently being manufactured commercially that have applications in the geosciences (e.g., Cameca's 1280, 7f, and NanoSIMS, ASI's SHRIMP and SHRIMP RG, EAG's ToF SIMS). Most of these instruments are characterized by a source region in which the intensity, energy, and orientation of the primary beam (relative to the sample) are controlled. Ions generated by this process form the secondary beam and are subsequently transmitted within a continuous high vacuum environment to a mass spectrometer. Most SIMS instruments used for elemental and isotopic analyses function by accelerating ions produced in the source along a potential gradient, typically 10 KV, and then transferring these ions into the mass spectrometer. Details of the configuration of the mass spectrometer vary from one application to another, but all utilize both magnetic and electrostatic analyzers, commonly referred to as sectors. If the electrostatic analyzer (sector) precedes the magnetic sector, the design is referred to as forward geometry. The advantage of this configuration is that
Typical configuration of a reverse geometry SIMS, the SHRIMP RG ion microprobe. Click image to enlarge. Details
the electrostatic filter reduces the energy range of the secondary ions so that they can then be separated into independent ion beams (based on the charge/mass ratio) by passing them through a magnetic field (magnetic sector). In this configuration, multiple ion beams can be measured simultaneously. If the magnetic sector precedes the electrostatic sector (reverse geometry), then mass resolution is improved at the cost of losing the ability to measure multiple ion beams simultaneously. Other types of mass spectrometers can be coupled to the SIMS source, including quadrupole and time-of-flight analyzers. These latter configurations have fewer applications in the geosciences.


SHRIMP RG at the Stanford-USGS Microanalytical Center (SUMAC). Details
In geochemistry SIMS is the instrumentation of choice for several analytical tasks, most noteworthy are:
  1. Large radius forward and reverse geometry instruments have been developed that can measure trace elemental and isotopic compositions in individual minerals with a spatial resolution down to roughly 10 microns. These applications include U-Th-Pb geochronology of zircon and other accessory minerals (e.g., SHRIMP).
  2. Large radius, double focusing instruments are also capable of measuring the isotopic composition of low atomic number elements such as O with similar spatial resolution (e.g., Cameca 1280) or even less for major constituents (e.g., 50 nanometers; NanoSIMS by Cameca Instruments)
  3. Smaller radius, double focusing instruments offer very high sensitivity (detection limits) for trace element analyses, roughly 10x the sensitivity of microprobes that utilize beams of electrons (e.g., Cameca IM 7f). These instruments can also used to "map" the distribution of individual elements in a sample.
  4. Some SIMS utilize other types of mass spectrometers (e.g., time-of-flight, quadrupole) and are used primarily for surface characterization, molecular analysis, and depth profiling.

Strengths and Limitations of Secondary Ion Mass Spectrometer (SIMS)?


The primary advantages of SIMS include:
  1. The analysis consumes very little sample (essentially non-destructive); for example, a typical U-Th-Pb analysis only consumes a few cubic micrometers of sample.
  2. High sensitivity also means that samples with low concentration levels (down to ppb levels) can be analyzed with SIMS. As a result, the SIMS is used to determine trace element abundances in meteorites, interplanetary dust, and other samples of limited size and are widely in the semiconductor industry to identify trace constituents in non-conducting substrates.
  3. High sensitivity also allows for depth profiling of elemental and molecular abundances as well as isotopic ratios.
  4. In situ analysis eliminates the need for complex sample preparation in most cases, i.e., minerals may be analyzed directly either as grain mounts or in thin sections.


Because both atomic and molecular species are produced during sputtering of the samples, not all elements in all substrates (matrices) can be analyzed quantitatively. For example, Lu-Hf in zircon is plagued by unresolvable isobaric (equal mass ions) interferences that cannot be overcome by either forward geometry multi-collection or reverse geometry high-resolution instruments. SIMS instrumentation tends be expensive, with typical instruments costing $2-3M.

User's Guide - Sample Collection and Preparation

As for all geochemical analyses, care must be taken to preserve sample integrity from the time of collection through analysis in all steps of physical and chemical preparation. In SIMS, care must be taken in the physical preparation of the sample prior to analysis. For SIMS the sample surface must be highly polished (~1 micrometer) and coated with a conducting, pure metal (particularly for non-conducting specimens) to avoid charge buildup on the surface. Failure to do so that can alter the behavior of the analyte ions and lead to erroneous results.

Data Collection, Results and Presentation

Quantitative isotopic and elemental data from this technique must be derived by comparing measurements of unknowns to well characterized standards. A key aspect of producing accurate, reproducible results, therefore, is identification and utilization of appropriate standards. For example, U-Th-Pb dating of zircon requires alternating analyses of unknown zircons with standard zircons in order to determine accurate U/Pb ratios and ages.


The following literature can be used to further explore Secondary Ion Mass Spectrometer (SIMS)

Recommended Readings:
  • Fitzsimons I.C.W., Harte B. and Clark R.M. (2000) SIMS stable isotope measurement: counting statistics and analytical precision. Mineral. Mag. 64 59-83
  • Hervig, R. L., Mazdab, F. K., Williams, P., Guan, Y., Huss, G. R., Leshin, L. A. (2006) Useful ion yields for Cameca IMS 3f and 6f SIMS: Limits on quantitative analysis. Chemical Geology, 227, 83-99.
  • Hinton R.W. (1990) Ion microprobe trace element analysis of silicates: Measurement of multi-element glasses. Chem. Geol. 83 11-25
  • Hinton, R. W. (1995) Ion Microprobe Analysis in Geology. IN: P.J. Potts, J.F.W. Bowles, S.J.B. Reed, and M.R. Cave (eds), Microprobe Techniques in the Earth Sciences. Chapman and Hall, pp 235-290.
  • Slodzian G. (1980) Microanalyzers Using Secondary Ion Emission. Advances in Electronics and Electronic Physics. Supplement 13B
  • De Laeter, John R.(2001) Mass spectrometry (including SIMS, ICP-MS, Accelerator MS, TIMS) Applications of inorganic mass spectrometry, John Wiley & Sons, New York, 474pp.
  • Swart P.K. (1990) Calibration of the Ion Microprobe for the Quantitive Determination of Strontium, Iron, Manganese and Magnesium in Carbonate Minerals.
  • Secondary Ion Mass Spectrometry: Basic Concepts, Instrumental Aspects, Applications, and Trends, by A. Benninghoven, F. G. Rudenauer, and H. W. Werner, Wiley, New York, 1987 (1227 pages).
Applications from the University of Wisconsin SIMS lab:
  • Page FZ, Ushikubo T, Kita NT, Riciputi LR, Valley JW (2007) High precision oxygen isotope analysis of picogram samples reveals μm gradients and slow diffusion in zircon. Am. Mineral. 92:1772-1775.
  • Kelly JL, Fu B, Kita NT, Valley JW (2007) Optically Continuous Silcrete Cements Of The St. Peter Sandstone: Oxygen Isotope Analysis By Ion Microprobe And Laser Fluorination. Geochem. Cosmochim. Acta. 71:3812-3832.
  • Cavosie AJ, Valley JW, Wilde SA, EIMF (2006) Correlated microanalysis of zircon: Trace element, δ18O, and U-Th-Pb isotopic constraints on the igneous origin of complex >3900 Ma detrital grains. Geochim Cosmochim Acta 70: 5601-5616.
  • Valley JW (2001) Stable Isotope Thermometry at High Temperatures: In: Valley JW and Cole DR (eds). Stable Isotope Geochemistry, Reviews In Mineralogy and Geochemistry, vol. 43, p. 365-414.
  • Valley, J. W., Graham, C. M., Harte, B., Kinny, P., and Eiler, J. M. (1998) Ion microprobe analysis of oxygen, carbon, and hydrogen isotope ratios. In: McKibben, M.A., et al. (eds), Soc. Econ. Geol. Rev. in Econ. Geol. 7, 73-98.
  • Eiler, J. M., Graham, C., and Valley, J. W. (1997) SIMS analysis of oxygen isotopes: matrix effects in complex minerals and glasses. Chemical Geol. 138, 221-244.
  • Valley, J. W. and Graham, C. M. (1991) Ion microprobe analysis of oxygen isotope ratios in metamorphic magnetite-diffusion reequilibration and implications for thermal history. Contr. Mineral. Petrol. 109, 38-52.

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