Sci. Rep. Kanazawa Univ.
Vol.48, No.1,2, p.43-71, 2004

43

The solution introduction ICP-MS techniqueto trace element analysis of rocks
Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU,
Yoshito ISHIDA, Yohei SHIMIZU and Tomoaki MORISHITA
Department of Earth Sciences, Faculty of Science, Kanazawa University, Kanazawa,
920-1192, Japan
Abstract : The solution introduction ICP-MS technique for trace element analysis ofrock samples was constructed at Kanazawa University. Trace element concentrations ofgeological standards (JB-2, JP-1, JA-1, and JGB-2) and Avacha peridotite xenoliths,
Russia, which are strongly depleted in major elements and the hardest matter for analysis,
were determined by the ICP-MS equipment. The values of concentration of middle toheavy masses (Rb-U) in geological standards coincide with those reported by other studies with ICP-MS techniques. The reproducibility is within 5 % of differences of valuesof Rb to Hf in JB-2 in response to the changes in dates, dilutions and calibration methods. In the case of peridotites (low trace elements concentrations in the order of ppb to
sub-ppb), relative standard deviations and relative differences among the runs under thevarious conditions are larger than in basalt with trace element concentrations in the orderof ppm. Especially, large relative standard deviations (> 10s %) for alkaline elements (Li,Rb, Cs), HFSE (Zr, Nb, Ta), Pb and Bi are shown in the refractory Avacha peridotite
xenoliths with trace element concentrations in the order of sub-ppb. The solution introduction ICP-MS technique is a powerful tool for a precise insight into trace element
characteristics of rocks of wide chemical compositions.

1. Introduction
Trace-elements characteristics of geological materials give us very important information about their constitutions, origins, histories and others. Because of the low concentrations as ppb-ppt orders of those elements in the geological material like peridotite, theirprecise determination is sometimes difficult and time consuming. Number of datasets oftrace elements in peridotite has increased from 1990’s due to improvement of technique of
inductively coupled plasma mass spectrometry (ICP-MS) (cf. Ionov et al., 1992; Ionov etal., 1993; Ionov et al., 1995; Bedini et al., 1999; Takazawa et al., 2003), which enables
us to measure trace elements with more than sub-ppt order concentrations.
ICP-MS, X7 (Thermo Electron Corporation, UK) was installed at the Department ofEarth Sciences, Kanazawa University in March, 2003. In order to measure trace-element
concentrations of rock samples, especially basalt and peridotite, we established the solution
introduction ICP-MS technique and examined reproducibility of results and consistency

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

with other studies.
2. Analytical techniques
2.1. Samples
In order to compare ICP-MS techniques between this study and the previous studies,
we analyzed the following geological standards prepared by the Geological Survey of Japan: JB-2, basalt from the Oshima volcano, Japan; JP-1, peridotite (dunite) from Horoman, Japan; JA-1, andesite from the Hakone volcano, Japan; JGb-2, gabbro from Mt.
Tsukuba, Japan. In order to check to our ability to determine the trace element concentrations in refractory peridotite with low trace element contents, we analyzed 6 peridotite(harzburgite) xenoliths from Avacha (Avachinsky) volcano in Kamchatka, Russia (AX-10，
-106，
-159，
-213，
-629，
-729). The Avacha peridotite is extremely refractory (Fo of olivine,
91-93; Cr# = Cr / (Cr + Al) of spinel, 0.5-0.8) (Arai et al., 2003) and may be the hardest
material from trace element analysis.
2.2. Sample preparation
De-ionized water, further purified (18.2 MΩ resistivity) by a milli-Q Element A-10
system (Millipore, Japan), was used throughout the procedure. All acids are of Ultrapur
grade (Kantokagaku, Japan).
R Teflon○
R beakers,
Rock powders of 100 mg were weighted into screw-cap Savillex○
and 1 ml of HNO3, 1 ml of HClO4 and 1.5 ml of HF were added to each sample. This
beaker was agitated in an ultrasonic bath in 10 minutes, and then the sample was heated todissolve at 110°
C in 3-7 days. The solution obtained was evaporated to achieve near dryness at 110°
C in 9-12 hours. After evaporation, 1 ml of HNO3 was added to the sample.
The beaker was capped again and heated at 110°
C in more than 2 hours. Moreover, 4 ml ofwater was added to the sample and heated again at 110°
C in more than 4 hours. This soluR PFA volumetric flask (VIT-LAB,
tion was diluted with water to 100 ml by using a Teflon○
Germany). In the case of the sample with dilution factor of more than 1000 times, the solution was further diluted with 1.2 % HNO3 in a test tube. Three solution samples were produced for each rock sample
A rock blank was prepared as follows. Water was “grinded” in an agate mortar, andR Teflon○
R beaker. At 110°
was poured into a screw-cap Savillex○
C, this beaker was driedup completely. Addition of acids to the rock blank and the subsequent preparations weresimilar to those for a rock sample.
2.3. Instrumentation and data acquisition
The ICP-MS used in this study is X7 (Thermo Electron corporation, UK) installed at
Kanazawa University. Details of operating conditions are shown in Table 1. An autosampler was used to supply the ICP-MS with samples, standards and wash acid. The system is

The solution introduction ICP-MS technique to trace element analysis of rocks

45

optimized to give a sensitively of approximately 120,000 cps for 115In in a 1 ng・ml-1 tuning
solution and a yield for CeO+ formation of about 3 %.
Data were acquired using software supplied by the manufacturer in peak jumping
mode: number of peak jump sweeps, 50; points per peak, 3; numbers of separation in
atomic mass unit, 50; collector type, pulse counting; and dwell time shown in Table 2.
Mixed standard solutions were prepared from ATX-1，-7，-8, and-13 (SPEX, USA).
Internal standardization
In order to correct for signal drift during each analytical run, 1ppb of 115In was used
for all masses. The internal standard, In 1 ppb, was added to standards, rock blanks andsamples. The sensitivity of 1 ppb In in a solution represents R . We estimate intensity of anelement in a solution by internal standard correction, Ici , as follows:
Ici = I / (R / Rb) ---(1)where I is the present intensity of the element in the solution, and Rb is sensitivity of In in
the standard blank.
Calibration methods
The sensitivities of all elements were examined by external calibration in standard solutions. Calibration lines for each element were drawn through three points of calibration(0.1, 1 and 10 ppb) and the point of origin. The corrections for intensities in standards,
samples and rock blanks were accomplished prior to estimations of concentrations. Because the concentration of each element in the standard blank is defined as 0 ppm, an intensity of an element in a solution, Icb, is subtracted by the intensity in the blank, Ib, from a intensity estimated by internal standard correction,
Icb = Ici - Ib．
---(2)The sample solution corrected by removal contamination during preparation is shown as
Ic = Icbi - Icbrb---(3)
where Icbrb is Icb of the rock blank.
In some samples, quantitative determinations of element concentrations were performed by the standard addition method. Calibration lines for each element are drawn
through the points of the addition standard (1 ppb) to the sample and the point of the zero
addition standard to the sample. In the case of standard addition method, the Ib is an intenTable 1. X7 operating conditions.

Table 2. Data acquisition characteristics and detection limits (D.L.). Individual detection limits with dilution factors of rockblanks are shown in sub-columns.

46
Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITAThe solution introduction ICP-MS technique to trace element analysis of rocks

47

sity of an element in the rock blank. An intensity of an element in the zero addition standard to the sample or the addition standard to sample is corrected as follows:---(4)
Ic = Ici - Ib．
The sequence of an analytical run
Analyses of the 3 % HNO3 and the following blank proceeded to analyses of agroup of sub-samples, standards or rock blanks. The 3 % HNO3 was used to wash out
memory effects. In order to examine signal drifts of elements through the run, the blankcorrection in a sample or a rock blank is generally as follows:---(5)
Ic = Ici - Ibi
where Ibi is the calculated intensity by internal standard correction in the preceding blank.
A sample list in the run 031104 is given in Table 3 as an example. Blanks were analyzed in both before and after analyses of each group of sub-samples, standards and rockblanks to investigate signal variations of elements throughout the run 031104. Original intensities are shown in Figure 1. Intensities of all elements in the blank (the order 7 in Table3) after analysis of standards increased in counts comparing with the blank in the order 2, i.
e. before analysis of standards. The treatment of 3 % HNO3 in the order 8 suppressed theincreases of counts in REE, Hf, Ta, Pb, Bi, and Th afterward. Memory effects were partly
washed out for Li, Rb and Cs, but the counts for these elements are higher than those inblank in the order 2 before analysis of standards. These intensities of rock blanks in the orders 10 to 12 are corrected as follows:
Icbrb = Ici (rock blank) - (Ibi (the order 9) + Ibi’ (the order 13)) / 2． ---(7)The corrected intensities of other elements for rock blanks are as the equation (6).
The blank after analysis of sub-samples was in higher intensity of V than those before
their analysis. The V intensity of sample is corrected as follows:
Ic = Ici (sample) - Ici (the blank before sub-samples)．
---(8)
Memory effects of Sc appeared after analysis of peridotite xenoliths (x 5,000). Also theanalysis of JB-2 (x 10,000) left memory effects of Rb, Sr, Y, Zr, Ba and Cs. Basically, theintensities of these elements are corrected by the equation (6). Because contents of Sr, Y,
Zr and Ba were different between jars A and B, corrected intensities in the JB-2 are represented by ;Ic = Ici (JB-2) - Ici (the blank in the order 25)．
---(9)
Memory effects of Li, Be, Rb and Cs were related not only with analyses of standards in the run 031104 but also with former runs. The Li, Be, Rb and Cs in the blank decreased simply in counts from the highest intensities in the order 7 to 400, 7, 1200 and 600,
respectively, with time through the run 031104. These intensities of samples are corrected
as follows:
Ic = Ici (sample) - (Ici (the blank before sub-samples)- Ici (the blank after sub-samples)) / 2． ---(10)Intensities in sub-samples that were kept constant with time between the blank analy-

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Table 3. The sample list in the run 031104 for analysis of Avacha peridotite xenoliths (AX-106, -10 and-213). The blank was divided into two jars (A and B).

The solution introduction ICP-MS technique to trace element analysis of rocks

49

Figure 1 Profiles of intensities corrected for internal standard in blanks in the run 031104 (Table 3).
Filled circle; the blanks in jar A analyzed before standards, rock blanks and samples. Filledsquare; the blanks in jar A analyzed after standards, rock blanks and samples. Opened diamond; the blanks in jar B. cps; counts per second

50Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Figure 1 (continued)

The solution introduction ICP-MS technique to trace element analysis of rocks

Figure 1 (continued)

51

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Table 4. Measured trace element concentrations (ppm), precision estimates, reference values, and working values for JB-2. ES and SA mean external standard calibration method and standard addition calibration method, respectively. Italic numbers indicate values above higher limits ofconcentrations of calibration lines. The values with asterisks in reference denote preferable
values.

ses are corrected by the equation (6). The blank of the jar B had higher contents of Sr, Y,
Zr and Ba and lower contents of Ce, Pb, Bi and Th than that of the jar A. These element intensities in the blank of the jar B are corrected as follows:
Ici’ = Ici (the blank of the jar B) - (Ici (the blank in the order 47)- Ici (the blank in the order 43))．
---(11)
Detection limits
A detection limit (DL) of an element is calculated as follows:
DL = 3 x (Icb x (dwell time))0.5 / A---(12)

The solution introduction ICP-MS technique to trace element analysis of rocks

53

where A is sensitivity of the element. Datasets of detection limits in standard blanks androck blanks are listed in Table 2. The standard blanks have detection limits of the order of
ppt for Sc and Ba and of the order of sub-ppt for the other elements. Detection limits of allelements in rock blanks increase from the order of sub-ppb to ppb with increasing the dilution factor from 1,000 to 100,000 times.
Dilution factors
We determined the extent of dilution from values of concentration of calibration standards, intensities below 2 x 106 cps (counts per seconds) under the pulse counting of detec-

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Table 5. Measured trace element concentrations (ppm), precision estimates, reference values, and working values for JP-1. ES and SA mean external standard calibration method and standard addition calibration method, respectively. Italic numbers indicate values above higher limits ofconcentrations of calibration lines. The values with asterisks in reference denote preferable values.

tor and detection limits. Generally, the dilution factor grows larger as the sample has higher
trace element contents. In this study, basically, we adopted the dilution factor of 1,000 or
5,000 times for peridotites and of 10,000 for basalt, gabbro and andesite.
3. Results and discussion
The values of trace-element concentrations for all rock samples are listed in Tables 4
to 8. In the case of basalt (JB-2), gabbro (JGb-2) and andesite (JA-1), the relative standard
deviation (RSD) is lower than 5 % for Rb, Sr, Y, Cs, REE, Pb, Bi, Th and U. The RSD is
up to several tens percent for HFSE (Zr, Nb, Hf and Ta). The RSD of all elements examined are lager in peridotite (JP-1 and AX) than in basalt, gabbro and andesite.

The solution introduction ICP-MS technique to trace element analysis of rocks

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Table 6. Measured trace element concentrations (ppm), precision estimates, reference values, and working values for JA-1. ES and SA mean external standard calibration method and standard addition calibration method, respectively. Italic numbers indicate values above higher limits ofconcentrations of calibration lines. The values with asterisks in reference denote preferable values.

3. 1. Reproducibility
In order to investigate reproducibility in response to differences of date, calibration
method and dilution factor, we analyzed the same samples, JB-2 and JP-1, under the various conditions.
Difference in date
The JB-2 solution with dilution factor of 10,000 was analyzed through 5 analyticalruns using the external standard calibration method. The differences of concentration
among analytical runs are shown in Figure 2. While the relative differences of light-masselements (Li-Ni) range from 0.7 to 1.3, the concentrations of middle- to heavy-mass ele-

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Table 7. Measured trace element concentrations (ppm), precision estimates, reference values, and working values for JGb-2. ES and SA mean external standard calibration method and standard addition calibration method, respectively. Italic numbers indicate values above higher limits ofconcentrations of calibration lines.

ments except Ta are stable within 10 % of relative differences. The analysis of JB-2 in therun 030924 is inferred to fail in the last sample preparation, because it yielded clearlylower concentrations of REE than in the other runs.
In the runs 030829, 030902 and 030919, dwell time of Ta was 0.1 seconds, whereas
the other runs were performed under the condition of 0.5 seconds of the Ta dwell time. In
the following discussion, the concentration of Ta in the run 031030 is a representativevalue for JB-2 using the external calibration method under the dilution factor of 10,000.

The solution introduction ICP-MS technique to trace element analysis of rocks

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Difference in dilution factor
In the case of using external standard calibration method, the JB-2 solution preparedwith a dilution factor of 50,000 in the run 030919 resulted in concentrations in Li, Be, Ni,
Cr, Ta, Th and U showing > 10 % differences to the solution with a lower dilution factor (x10,000). The REE concentrations show the differences within 3 %. The large differences
for the former elements are due not to an error of sample dilution but to the difference ofconcentration between blanks.
The limits of determinations of values depend on the dilution factors in the case of using standard addition calibration method in this study. Analyses of JB-2 solutions withvarious dilution factors (x 10,000, 50,000, 100,000) yield various Sc, V, Sr, Ba concentrations in the run 031003 (Table 4). However, most of the elements concentration determined below higher limits of concentration in calibration lines show < 5 % of relative differences among solutions in this run. These results indicate that a value without a calibration line is possibly doubtful.
Difference in calibration method
Comparing two types of calibration method in the JB-2 solution with dilution factorof 10,000, the concentrations of elements from Cr to Ta have relative differences within 5%.
Summary of the reproducibility of JB-2 analysis
The concentrations of middle-mass elements (Rb-Hf) without one outer calibrationline can be reproduced even if we change date of analysis, dilution factor (x 10,000 or
50,000), and calibration method. Light-and heavy-mass elements concentrations, however,show various values within 50 % of relative differences.
The reproducibility of peridotite
Incompatible trace-element concentrations are generally lower in peridotite than in basalt. In order to examine the reproducibility for trace-element analysis of peridotite, JP-1
and Avacha peridotite xenoliths were analyzed with various calibration methods and dilution factors (x 1,000 or 5,000). The relative differences among the runs are plotted in Figures 3 and 4. Most of the values of concentrations determined in the peridotite solutions arein < 15 % of relative differences to those obtained with a dilution factor of 1,000 by using
external standard calibration method. In some cases, the values of alkaline elements (Li, Rb,
Cs), HFSE (Zr, Nb, Hf, Ta), Pb, Bi, Th and U are dispersed among the runs under the various conditions. The dispersion for alkaline elements and HFSE is different in manner from
JB-2, and possibly being due either to memory effects or to contamination of blanks.

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Table 8. Measured trace element concentrations (ppm) for Avach peridotite xenoliths (AX-10, -106,-159, -213, -629 and -729). ES and SA mean external standard calibration method and standard addition calibration method, respectively.

3. 2. Comparisons with other working values of geological standards
The relative differences of values of concentration in the run 030829 (external standard calibration method; dilution factor of 10,000 for JB-2, JA-1 and JGb-2 and of 1,000
for JP-1) of this study and previous studies using ICP-MS technique from the reference
values (Imai, 1995), which were mainly determined to be mean values of reviewed datasets
until 1991, are shown in Figures 5 to 8. In the case of JB-2 and JA-1, the relative differences in most of middle- to heavy-mass element concentrations determined by ICP-MS
techniques including this study are confined within 20 % from the reference values (Figs. 5
and 7). Although the values of middle- to heavy-masses are different from reference values
for JP-1 and JGb-2 (Figs. 6 and 8), the results in this study coincide well with other studies
by ICP-MS technique.
The Nb values of all geological standards are commonly much lower than the reference values (Figs. 5 to 8). The values of Nb of JB-2 by various techniques are shown inThe solution introduction ICP-MS technique to trace element analysis of rocks

59

Figure 9 for comparison. The values determined by ICP-MS techniques are confinedwithin narrow range from 0.43 to 0.8 ppm. In contrast the values determined by XRF arescattered from 0.2 to 3.8 ppm encompassing the range of ICP-MS data.
In JP-1, the values determined by ICP-MS techniques are lower than reference values.
The values of La for JP-1 by various techniques are shown in Figure 10 as an example.
They range widely from 0.025 to 27 ppm. The La values determined by ICP-MS techniques range narrowly again from 0.025 to 0.043 ppm, that is nearly the lowest of all
ranges obtained by various techniques (Fig. 10). This indicates that the values of trace elements in JP-1 can be reproduced well under the various conditions (laboratory, machine
and user), whereas they have been overestimated in some previous studies using othertechniques because of their low concentrations (< 10s ppb).

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Table 8
(continued)

4. Summary and conclusions
We have constructed the solution introduction ICP-MS technique at Kanazawa University, and determined the trace element concentrations in geological standards and peridotite xenoliths by this technique. The values of Rb to Hf in JB-2 in this study show reproducibility within 5 % of differences under the various conditions for changes in date ofanalysis, dilution factor and calibration method. In the case of peridotite with low traceelement concentrations, relative standard deviations and relative differences among theruns under the various conditions are larger than in basalt. The lowest detection limits arein the order of sub-ppb for rock blanks, but alkaline elements (Li, Rb, Cs), HFSE (Zr, Nb,
Ta), Pb and Bi show dispersed values of concentration in the order of ppb.
The values of concentration of middle- to heavy-masses (Rb-U) in geological standards of this study coincide with those from other studies with ICP-MS techniques. The
advantages of ICP-MS technique in comparison with other techniques are the excellent re-

The solution introduction ICP-MS technique to trace element analysis of rocks

61

Figure 2 Relative differences (R.D.s) of the trace-element concentration in JB-2 under various conditions from the values determined by the run 030829: the external standard calibration methodwith a dilution factor of 10,000.

Figure 3 Relative differences (R.D.s) of the trace-element concentration in JP-1 under various conditions from the values determined by the run 030829: the external standard calibration methodwith a dilution factor of 1,000.

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Figure 4 Relative differences (R.D.s) of the trace-element concentration in Avacha peridotite xenoliths
under various conditions from the values determined by the external standard calibration
method with a dilution factor of 1,000. Opened circle; the external standard calibration
method, dilution factor of 5,000. Filled circle; the standard addition calibration method with adilution factor of 5,000.

The solution introduction ICP-MS technique to trace element analysis of rocks

Figure 4 (continued)

63

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Figure 4 (continued)

The solution introduction ICP-MS technique to trace element analysis of rocks

65

Figure 5 Relative differences (R.D.s) of working values including the run 030829 (the external standard
calibration method with a dilution factor of 10,000) in this study to the reference values of
Imai et al. (1995) for JB-2.

Figure 6 Relative differences (R.D.s) of working values including the run 030829 (the external standard
calibration method with a dilution factor of 1,000) in this study to the reference values of Imaiet al. (1995) for JP-1.

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Figure 7 Relative differences (R.D.s) of working values including the run 030829 (the external standard
calibration method with a dilution factor of 10,000) in this study to the reference values of
Imai et al. (1995) for JA-1.

Figure 8 Relative differences (R.D.s) of working values including the run 030829 (the external standard
calibration method with a dilution factor of 10,000) in this study to the reference values of
Imai et al. (1995) for JGb-2.

The solution introduction ICP-MS technique to trace element analysis of rocks

67

Figure 9 A comparison of the values of Nb concentration in JB-2 by various techniques. The list ofworking values from literature is given in Table 9. The reference value is from Imai et al.
(1995)

Table 9. A list of values of Nb in JB-2 by previous studies and the present study.

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Miki SHIRASAKA, Shoji ARAI, Satoko ISHIMARU, Yoshito ISHIDA,
Yohei SHIMIZU and Tomoaki MORISHITA

Figure 10 A comparison of the values of La concentration in JP-1 by various techniques. The list ofworking values with references is given in Table 10. The reference value is from Imai et al.
(1995)
Table 10. A list of the values of La in JP-1 by previous studies and the present study. Details of references are given in GSJ homepage.

The solution introduction ICP-MS technique to trace element analysis of rocks

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producibility despite of various analytical conditions and the sensitivity to determine traceelement concentrations as low as in the order of sub ppt to ppb. The solution introduction
ICP-MS technique established in this study is powerful tool for analysis of geological andenvironmental processes and materials based on trace-element geochemistry.
Acknowledgments
We acknowledge Associate Prof. J. Kimura of Shimane University, Associate Prof. E.
Takazawa of Niigata University and Dr. Y. Orihashi of University of Tokyo for their advice about the solution introduction ICP-MS technique to geological samples. We are also
grateful to Ms. T. Takahashi, Mr. T. Iyama and Mr. S. Simon of Thermo Electron Corporation for their supplying basic information about the solution introduction ICP-MS technique with us. The ICP-MS system was installed in the course of research by the 21stCentury COE project “Environmental Monitoring and projection of Long-and Short-Term
Dynamics of Pan-Japan Sea Area: Construction of Monitoring Network and Assessmentof Human Effects” led by Prof. K. Hayakawa, Kanazawa University. We express our deepest appreciation to Prof. K. Hayakawa for his leadership.
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