1. TAKADA Masashi (Nara Womens University, Japan : takada@cc.nara-wu.ac.jp TAKADA Masashi (Nara Womens University, Japan : takada@cc.nara-wu.ac.jp 1. INTRODUCTION In Luminescence dating, the principal minerals mostly used are quartz and feldspar. However, tephra and lava originated from mafic magma seldom contain quartz and volcanic feldspar often shows anomalous fading (Aitken, 1985). It practically inhibits luminescence dating. Olivine ([Mg,Fe] 2 SiO 4 ) is one of the common minerals included in igneous rocks such as basalt, diabase and gabbro which seldom contain quartz. Olivines vary in chemical composition from forsterite (Fo100; Mg 2 SiO 4 ) to fayalite (Fo0; Fe 2 SiO 4 ), there being complete diadochy between Mg 2+ and Fe 2+ in the structure (Deer et. al., 1966). Though Koike et al. (2002) clarified some luminescence properties of forsterite as interstellar matter within the low temperature environment, little had been known about ones of natural olivine from geological sites. Therefore Takada et al. (2006) preliminarily studied on TL and OSL behavior of olivine relative to dosimetry and Cenozoic dating. Olivine ([Mg,Fe] 2 SiO 4 ) is one of the common minerals included in igneous rocks such as basalt, diabase and gabbro which seldom contain quartz. Olivines vary in chemical composition from forsterite (Fo100; Mg 2 SiO 4 ) to fayalite (Fo0; Fe 2 SiO 4 ), there being complete diadochy between Mg 2+ and Fe 2+ in the structure (Deer et. al., 1966). Though Koike et al. (2002) clarified some luminescence properties of forsterite as interstellar matter within the low temperature environment, little had been known about ones of natural olivine from geological sites. Therefore Takada et al. (2006) preliminarily studied on TL and OSL behavior of olivine relative to dosimetry and Cenozoic dating. In this presentation, the author reports the practical application of luminescence from natural olivine to Quaternary dating of volcanic rocks. In this presentation, the author reports the practical application of luminescence from natural olivine to Quaternary dating of volcanic rocks. 3. SAMPLE PREPARATION Firstly I used specimens of pure olivine crystals from Arizona, U.S.A. to check etching condition (Figures 1 and Table 1and internal dose. Secondly I tried to extract olivine crystals from volcanic rocks in the Hakkoda-san district, northern Japan (Figures, 4 and Tables 2, 3). The procedures of the sample preparation and TL measurements are shown in Figures and 5. 3. SAMPLE PREPARATION Firstly I used specimens of pure olivine crystals from Arizona, U.S.A. to check etching condition (Figures 1 and Table 1 ) and internal dose. Secondly I tried to extract olivine crystals from volcanic rocks in the Hakkoda-san district, northern Japan (Figures, 4 and Tables 2, 3). The procedures of the sample preparation and TL measurements are shown in Figures and 5. Fig.. Location of volcanic samples 5. REFERENCES Aitken, M.J., 1985. Thermoluminescence dating. Academic Press, 359pp. Aitken, M.J., 1985. Thermoluminescence dating. Academic Press, 359pp. Deer, W.A., Howie, R.A. and Zussman, T., 1966. An introduction to the rock forming minerals. Longman, 528pp. Deer, W.A., Howie, R.A. and Zussman, T., 1966. An introduction to the rock forming minerals. Longman, 528pp. Koike, K., Nakagawa, M., Koike, C., Okada, M. and Chihara, H., 2002. Thermoluminescence of Simulated Interstellar Matter after Gamma-ray Irradiation. Astronomy & Astrophysics, 390, 1133-1139. Koike, K., Nakagawa, M., Koike, C., Okada, M. and Chihara, H., 2002. Thermoluminescence of Simulated Interstellar Matter after Gamma-ray Irradiation. Astronomy & Astrophysics, 390, 1133-1139. Takada, M., Tani, A. and Shimada, A., 2006. Preliminary study of the application of natural olivine in Cenozoic dating. Radiation Measurements, 41, 982-986. Takada, M., Tani, A. and Shimada, A., 2006. Preliminary study of the application of natural olivine in Cenozoic dating. Radiation Measurements, 41, 982-986. P-H4 2. TL MEASUREMENT TL measurements were made on an automated RISO TL/OSL-DA15 reader mounted with an integral 90 Sr- 90 Y beta source. Photon counting used a Thorn-EMI 9235 QA photomultiplier tube coupled to HA-30 and BG7-59 detection filters (290-480 nm transmission) for TL. Optical stimulation were performed using blue LEDs (475±45 nm, power of 15 mW/cm to the sample). Fig. 1 Relationship between etching time (minutes) and residual weight (%) of olivine specimens from Arizona, U. S. A. 1) Immersion in 10% hydrofluoric acid 4. RESULTS AND DISCISSIONS Figure 1and Table 1suggest immersion in 10% hydrofluoric acid for about 30 minutes allows etching of the outer layer of the olivine grains to a depth sufficient for the cores remaining to have a negligible component of alpha particle dosage. Alpha counting of the olivine specimen suggests the internal dose from olivine is negligible. Modified SAR protocol for TL measurements of olivine extracted from Ohsegawa pyroclastic flow deposits give TL ages but they are disperse and underestimated (Figs. 5, 6, 7 and Table 4). The reasons are unknown at present but further studies on sensitivity change and fading behaviour of olivine are needed. 4. RESULTS AND DISCISSIONS Figure 1 and Table 1 suggest immersion in 10% hydrofluoric acid for about 30 minutes allows etching of the outer layer of the olivine grains to a depth sufficient for the cores remaining to have a negligible component of alpha particle dosage. Alpha counting of the olivine specimen suggests the internal dose from olivine is negligible. Modified SAR protocol for TL measurements of olivine extracted from Ohsegawa pyroclastic flow deposits give TL ages but they are disperse and underestimated (Figs. 5, 6, 7 and Table 4). The reasons are unknown at present but further studies on sensitivity change and fading behaviour of olivine are needed. Table 1a. Assumed crystalline form : Octahedron Depth of a removed outer layer a-axisb-axisc-axisVolume Residual ratio μ (mm 3 ) ( ) 04.00000 21.33333 3 100.00% 13.99717 21.28811 0 99.79% 23.99434 21.24295 2 99.58% 33.99151 21.19785 7 99.36% 43.98869 21.15282 6 99.15% 53.98586 21.10785 8 98.94% 63.98303 21.06295 5 98.73% 73.98020 21.01811 5 98.52% 83.97737 20.97333 9 98.31% 93.97454 20.92862 6 98.10% 103.97172 20.88397 7 97.89% 113.96889 20.83939 2 97.68% 123.96606 20.79487 0 97.48% 133.96323 20.75041 2 97.27% 143.96040 20.70601 7 97.06% 153.95757 20.66168 5 96.85% 163.95475 20.61741 7 96.64% 173.95192 20.57321 2 96.44% 183.94909 20.52907 0 96.23% 193.94626 20.48499 2 96.02% 203.94343 20.44097 6 95.82% Table 1b. Assumed crystalline form : Globe Depth of a removed outer layer a-axisb-axisc-axisVolume Residual ratio μ (mm 3 ) ( ) 04.00000 33.50933 3 100.00% 13.99800 33.45909 4 99.85% 23.99600 33.40890 6 99.70% 33.99400 33.35876 7 99.55% 43.99200 33.30867 9 99.40% 53.99000 33.25864 1 99.25% 63.98800 33.20865 3 99.10% 73.98600 33.15871 5 98.95% 83.98400 33.10882 8 98.80% 93.98200 33.05899 0 98.66% 103.98000 33.00920 2 98.51% 113.97800 32.95946 5 98.36% 123.97600 32.90977 7 98.21% 133.97400 32.86013 9 98.06% 143.97200 32.81055 2 97.91% 153.97000 32.76101 4 97.77% 163.96800 32.71152 6 97.62% 173.96600 32.66208 8 97.47% 183.96400 32.61270 0 97.32% 193.96200 32.56336 1 97.18% 203.96000 32.51407 3 97.03% Table 1. Relationship between depth (μ of removed outer layer and residual volume/weight (%) of an olivine crystal Fig. 3. Sample preparation Table 4. TL ages of Ohsegawa pyroclastic flow deposits. Fig. 6. Fig. 4. Extracted olivine grains from Ohsegawa pyroclastic deposits Fig. 5. Modified SAR protocol for TL measurement N o. Sample name Sample code Location DepthCosmic Ray Reference Age (ka) LatitudeLongitudea.s.l. (m)(m)(Gy/ka) 1Arizona olivine----- - - 2Ohdake lavaHo1N40.63E140.83740>50.115±0.006 K-Ar 150-300 3 Ohsegawa pyroclastic flow deposit HtoN40.57E140.95300>1500.001±0.000 Stratigraphy and paleomagnetism 800-1,000 Table. Samples in this study Fig. 7. Regenerated growth curve of olivine extracted from Ohsegawa pyroclastic rocks.