Luminescence dating

Luminescence dating refers to a group of methods of determining how long ago mineral grains were last exposed to sunlight or sufficient heating. It is useful to geologists and archaeologists who want to know when such an event occurred. It uses various methods to stimulate and measure luminescence

It includes techniques such as optically stimulated luminescence (OSL), infrared stimulated luminescence (IRSL), and thermoluminescence (TL). "Optical dating" typically refers to OSL and IRSL, but not TL.

Conditions and accuracy

All sediments and soils contain trace amounts of radioactive isotopes of elements such as potassium, uranium, thorium, and rubidium. These slowly decay over time and the ionizing radiation they produce is absorbed by mineral grains in the sediments such as quartz and potassium feldspar. The radiation causes charge to remain within the grains in structurally unstable "electron traps". The trapped charge accumulates over time at a rate determined by the amount of background radiation at the location where the sample was buried. Stimulating these mineral grains using either light (blue or green for OSL; infrared for IRSL) or heat (for TL) causes a luminescence signal to be emitted as the stored unstable electron energy is released, the intensity of which varies depending on the amount of radiation absorbed during burial and specific properties of the mineral.

Most luminescence dating methods rely on the assumption that the mineral grains were sufficiently "bleached" at the time of the event being dated. For example, in quartz a short daylight exposure in the range of 1-100 seconds before burial is sufficient to effectively “reset” the OSL dating clock.[1] This is usually, but not always, the case with aeolian deposits, such as sand dunes and loess, and some water-laid deposits.

Quartz OSL ages can be determined typically from 100 to 350,000 years BP, and can be reliable when suitable methods are used and proper checks are done.[2] Feldspar IRSL techniques have the potential to extend the datable range out to a million years as feldspars typically have significantly higher dose saturation levels than quartz, though issues regarding anomalous fading will need to be dealt with first.[1] Ages can be obtained outside this these ranges, but they should be regarded with caution. The uncertainty of an OSL date is typically 5-10% of the age of the sample.[3]

History

The concept of using luminescence dating in archaeological contexts was first suggested in 1953 by Farrington Daniels, Charles A. Boyd, and Donald F. Saunders, who thought the thermoluminescence response of pottery shards could date the last incidence of heating.[4] Experimental tests on archaeological ceramics followed a few years later in 1960 by Grögler et al.[5] Over the next few decades, thermoluminescence research was focused on heated pottery and ceramics, burnt flints, baked hearth sediments, oven stones from burnt mounds and other heated objects.[3]

In 1963, Aitken et al. noted that TL traps in calcite could be bleached by sunlight as well as heat,[6] and in 1965 Shelkoplyas and Morozov were the first to use TL to date unheated sediments.[7] Throughout the 70s and early 80s TL dating of light-sensitive traps in geological sediments of both terrestrial and marine origin became more widespread.[8]

Optically stimulated luminescence (OSL) was developed in 1984 by David Huntley and colleagues.[9] Hütt et al. laid the groundwork for the infrared stimulated luminescence (IRSL) dating of potassium feldspars in 1988.[10]

In 1994, the principles behind optical and thermoluminescence dating were extended to include surfaces made of granite, basalt and sandstone, such as carved rock from ancient monuments and artifacts. Ioannis Liritzis, the initiator of ancient buildings luminescence dating, has shown this in several cases of various monuments.[11][12][13]

Physics

Luminescence dating is one of several techniques in which an age is calculated as follows:

age = (total absorbed radiation dose) / (radiation dose rate)

The radiation dose rate is calculated from measurements of the radioactive elements (K, U, Th and Rb) within the sample and its surroundings and the radiation dose rate from cosmic rays. The dose rate is usually in the range 0.5 - 5 grays/1000 years. The total absorbed radiation dose is determined by exciting specific minerals (usually quartz or potassium feldspar) extracted from the sample with light and measuring the amount of light emitted as a result. The photons of the emitted light must have higher energies than the excitation photons in order to avoid measurement of ordinary photoluminescence. A sample in which the mineral grains have all been exposed to sufficient daylight (seconds for quartz; hundreds of seconds for potassium feldspar) can be said to be of zero age; when excited it will not emit any such photons. The older the sample is, the more light it emits, up to a saturation limit.

Minerals

The minerals that are measured are usually either quartz or potassium feldspar sand-sized grains, or unseparated silt-sized grains. There are advantages and disadvantages to using each. For quartz, blue or green excitation frequencies are normally used and the near ultra-violet emission is measured. For potassium feldspar or silt-sized grains, near infrared excitation (IRSL) is normally used and violet emissions are measured.

Comparison to radiocarbon dating

Unlike carbon-14 dating, luminescence dating methods do not require a contemporary organic component of the sediment to be dated; just quartz, potassium feldspar, or certain other mineral grains that have been fully bleached during the event being dated. These methods also do not suffer from overestimation of dates when the sediment in question has been mixed with “old carbon”, or 14
C-deficient carbon that is not the same isotopic ratio as the atmosphere. In a study of the chronology of arid-zone lacustrine sediments from Lake Ulaan in southern Mongolia, Lee et al. discovered that OSL and radiocarbon dates agreed in some samples, but the radiocarbon dates were up to 5800 years older in others.[14]

The sediments with disagreeing ages were determined to be deposited by aeolian processes. Westerly winds delivered an influx of 14
C-deficient carbon from adjacent soils and Paleozoic carbonate rocks, a process that is also active today. This reworked carbon changed the measured isotopic ratios, giving a false older age. However, the wind-blown origin of these sediments were ideal for OSL dating, as most of the grains would have been completely bleached by sunlight exposure during transport and burial. Lee et al. concluded that when aeolian sediment transport is suspected, especially in lakes of arid environments, the OSL dating method is superior to the radiocarbon dating method, as it eliminates a common ‘old-carbon’ error problem.[14]

Notes

  1. 1 2 Rhodes, E. J. (2011). "Optically stimulated luminescence dating of sediments over the past 250,000 years". Annual Review of Earth and Planetary Sciences 39: 461–488. doi:10.1146/annurev-earth-040610-133425. Retrieved February 8, 2016.
  2. ↑ Murray, A. S. & Olley, J. M. (2002). "Precision and accuracy in the optically stimulated luminescence dating of sedimentary quartz: a status review" (PDF). Geochronometria 21: 1–16. Retrieved February 8, 2016.
  3. 1 2 Roberts, R.G., Jacobs, Z., Li, B., Jankowski, N.R., Cunningham, A.C., & Rosenfeld, A.B. (2015). "Optical dating in archaeology: thirty years in retrospect and grand challenges for the future". Journal of Archaeological Science 56: 41–60. doi:10.1016/j.jas.2015.02.028. Retrieved February 16, 2016.
  4. ↑ Daniels, F., Boyd, C.A., & Saunders, D.F. (1953). "Thermoluminescence as a research tool". Science 117 (3040): 343–349. doi:10.1126/science.117.3040.343. Retrieved March 15, 2016.
  5. ↑ Grögler, N., Houtermans, F.G., & Stauffer, H. (1960). "Über die datierung von keramik und ziegel durch thermolumineszenz.". Helvetica Physica Acta 33: 595–596. Retrieved February 16, 2016.
  6. ↑ Aitken, M.J., Tite, M.S. & Reid, J. (1963). "Thermoluminescent dating: progress report". Archaeometry 6: 65–75. doi:10.1111/j.1475-4754.1963.tb00581.x. Retrieved February 16, 2016.
  7. ↑ Shelkoplyas, V.N. & Morozov, G.V. (1965). "Some results of an investigation of Quaternary deposits by the thermoluminescence method". Materials on the Quaternary Period of the Ukraine. 7th International Quaternary Association Congress, Kiev: 83–90.
  8. ↑ Wintle, A.G. & Huntley, D.J. (1982). "Thermoluminescence dating of sediments". Quaternary Science Reviews 1: 31–53. doi:10.1016/0277-3791(82)90018-X. Retrieved February 16, 2016.
  9. ↑ Huntley, D. J., Godfrey-Smith, D. I., & Thewalt, M. L. W. (1985). "Optical dating of sediments". Nature 313: 105 – 107. doi:10.1038/313105a0. Retrieved February 16, 2016.
  10. ↑ Hütt, G., Jaek, I. & Tchonka, J. (1988). "Optical dating: K-feldspars optical response stimulation spectra". Quaternary Science Reviews 7: 381 – 385. doi:10.1016/0277-3791(88)90033-9. Retrieved February 16, 2016.
  11. ↑ Liritzis, I. (2011). "Surface Dating by Luminescence: An Overview". Geochronometria (Silesian University of Technology, Poland) 38 (3): 292–302. doi:10.2478/s13386-011-0032-7.
  12. ↑ Liritzis, I., Polymeris, S.G., and Zacharias, N. (2010). "Surface Luminescence Dating of 'Dragon Houses' and Armena Gate at Styra (Euboea, Greece)". Mediterranean Archaeology and Archaeometry 10 (3): 65–81.
  13. ↑ Liritzis, I. (2010). "Strofilas (Andros Island, Greece): new evidence for the cycladic final neolithic period through novel dating methods using luminescence and obsidian hydration". Journal of Archaeological Science (Elsevier) 37: 1367–1377. doi:10.1016/j.jas.2009.12.041.
  14. 1 2 Lee, M.K., Lee, Y.I., Lim, H.S., Lee, J.I., Choi, J.H., & Yoon, H.I. (2011). "Comparison of radiocarbon and OSL dating methods for a Late Quaternary sediment core from Lake Ulaan, Mongolia". Journal of Paleolimnology 45: 127–135. doi:10.1007/s10933-010-9484-7. Retrieved February 14, 2016.

References

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