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Archeointensity study on baked clay samples taken from the reconstructed ancient kiln: implication for validity of the Tsunakawa-Shaw paleointensity method
© Yamamoto et al.; licensee Springer. 2015
- Received: 16 January 2015
- Accepted: 14 April 2015
- Published: 8 May 2015
In 1972, a reconstruction experiment of a kiln had been done to reproduce an excavated kiln of the seventh century in Japan. Baked clay samples were taken from the floor surface and −20 cm level, and they have been stored after determinations of the paleomagnetic directions by partial alternating field demagnetizations. We recently applied the Tsunakawa-Shaw method to the samples to assess how reliable archeointensity results are obtained from the samples. A suite of the rock magnetic experiments and the scanning electron microscope observations elucidate that dominant magnetic carriers of the floor surface samples are Ti-poor titanomagnetite grains in approximately 10 nm size with single-domain and/or super-paramagnetic states, whereas contributions of multi-domain grains seem to be relatively large for the −20-cm level samples. From the floor surface samples, six out of the eight successful results were obtained and they give an average of 47.3 μT with a standard deviation of 2.2 μT. This is fairly consistent with the in situ geomagnetic field of 46.4 μT at the time of the reconstruction. They are obtained with a built-in anisotropy correction using anhysteretic remanent magnetization and without any cooling rate corrections. In contrast, only one out of four was successful from the −20-cm level samples. It yields an archeointensity of 31.6 μT, which is inconsistent with the in situ geomagnetic field. Considering from the in situ temperature record during the firing of the kiln and the unblocking temperature spectra of the samples, the floor surface samples acquired full thermoremanent magnetizations (TRMs) as their natural remanent magnetizations whereas the −20-cm level samples only acquired partial TRMs, and these differences probably cause the difference in the archeointensity results between the two sample groups. For archeointensity researches, baked clay samples from a kiln floor are considered to be ideal materials.
- Absolute paleointensity
- Baked clay
- Tsunakawa-Shaw method
Recent advances in archeomagnetism have resulted in sophisticated databases for published archeomagnetic data. For example, the GEOMAGIA50 database (Donadini et al. 2006; Korhonen et al. 2008) involves about 8,000 geomagnetic field directions and intensities for the past 50 kyr. The ARCH3k database by Donadini et al. (2009) contains 2,671 declination, 4,174 inclination, and 2,670 intensity data from archeological artifacts and lavas for the past 3 kyr. Genevey et al. (2008) compiled the Archeoint database for the past 10 kyr which has 3,648 archeointensity records reported from archeological artifacts and lavas.
Concerning the Archeoint database, 70% of the records are from Europe while only 12% of them are from East Asia. Among the East Asia records, 188 data are from Japan: 145 data from archeological artifacts (9 data, Nagata and Arai (1963); 19 data, Sasajima and Maenaka (1966); 56 data, Kitazawa (1970); 6 data, Domen (1977); 58 data, Sakai and Hirooka (1986)) and 43 data from lavas (7 data, Nagata and Arai (1963); 2 data, Sasajima and Maenaka (1966); 6 data, Kono (1978); 1 data, Tanaka (1979); 13 data, Tanaka (1980); 3 data, Tsunakawa and Shaw (1994); 1 data, Takai et al. (2002); 10 data, Yoshihara et al. (2003)).
In broad sense, ‘archeointensity’ stands for an absolute paleointensity of the geomagnetic field during historical period which is estimated from both archeological artifacts and lavas. In narrow sense, the estimation material is limited to archeological artifacts. Generally speaking, archeological artifacts have been considered to be more reliable paleointensity recorders, because they were certainly burned/baked by our ancestors and their natural remanent magnetizations (NRMs) are definitely thermoremanent magnetization (TRM) origin with good thermal stability.
There has been a long gap in time since the last internationally recognized archeointensity result was published from archeological artifacts in Japan (e.g., Sakai and Hirooka 1986). In contrast, brand new data with modern paleointensity techniques have been published from East Asia outside Japan, for example, Korea (Yu et al. 2010; Hong et al. 2013) and China (Cai et al. 2014). In 1960s to 1970s, a group of Japanese researchers had made systematic oriented-sample collections from baked clay at many pottery kilns excavated in and around Sakai city, Osaka prefecture, Japan. The collections were associated with a lot of excavations arising from a big demand of housing land developments due to the growing economy in Japan at that time. Paleomagnetic directions for fifth to tenth centuries were intensively measured from these samples, and they were published by Hirooka (1971) and Shibuya (1980). Untreated and/or partially demagnetized samples have been reserved and stored for further archeointensity (paleointensity) researches.
A relatively large number of the reserved samples were partially demagnetized by alternating field (AF) up to 20 to 40 mT. Thus, AF-based paleointensity techniques are thought to be suitable for these samples. The Tsunakawa-Shaw method, which has been previously called the LTD-DHT Shaw method (Tsunakawa and Shaw 1994; Yamamoto et al. 2003), is one of such techniques. Its applicability and validity have been elucidated for various types of volcanic rocks from historical lava flows (e.g., Yamamoto et al. 2003; Mochizuki et al. 2004; Oishi et al. 2005; Yamamoto and Hoshi 2008) but remain unassessed for archeological artifacts including baked clay.
In the vicinity of the archeological sites, Nakajima et al. (1974) conducted a reconstruction experiment: they reconstructed a kiln which was carefully imitating an excavated kiln of the seventh century and measured paleomagnetic directions from baked clay samples taken from the kiln. These samples have been reserved and stored after partial AF demagnetization by 20 to 40 mT in 1972. In the present study, we applied the Tsunakawa-Shaw method to these samples. Because the reconstruction experiment was done after the measurement of the in situ geomagnetic field, we can compare the in situ filed with archeointensity results obtained by the Tsunakawa-Shaw method. We also conducted a suite of rock magnetic experiments and an observation with scanning electron microscope, to characterize rock magnetic properties of the samples.
After cutting the trees and weeds (Figure 1a), the ground was dug up (Figure 1b). Then in situ geomagnetic field was measured by a Schmidt-type magnetometer (Figure 1c): declination (Dec) = −5.63°, inclination (Inc) = 46.78°, and intensity (Int) = 46.350 μT. This is fairly consistent with the field calculated from the model of IGRF-11 (IAGA Division V, Working Group V-MOD 2010) at the place for the year of 1972: Dec = −6.23°, Inc = 47.7°, and Int = 46.438 μT. To record in situ temperature variations during the firing, thermocouples were embedded in and around the kiln (Figure 1d,e). After the embedment, the body of the kiln was made up with bamboos and tree branches, and they were subsequently covered and coated with clay (Figure 1f). With Sue-type earthenwares, the firing was done using naturally grown pine trees and other miscellaneous woods taken around the kiln (Figure 1g,h).
The samples were subjected to partial AF demagnetization up to 20 to 40 mT. Nakajima et al. (1974) reported that the mean paleomagnetic directions resulted in Dec = −5.03°, Inc = 43.37°, and α95 = 2.42° for the floor surface samples (N = 10) and in Dec = −4.80°, Inc = 43.52°, and α95 = 3.38° for the −20-cm level samples (N = 5). These directions were reasonably consistent with the in situ geomagnetic field direction measured prior to the firing, though the mean inclinations were approximately 3° shallower than the in situ field.
Rock magnetic experiments
The hysteresis parameters, saturation magnetization (M s), saturation remanent magnetization (M rs), coercive force (B c), and coercivity of remanence (B rc) were measured for two to four chips from each sample, using a vibrating sample magnetometer (MicroMag 3900 VSM, Princeton Measurements Corporation, Princeton, NJ, USA). Thermomagnetic curve measurements were performed in vacuum (approximately 1 to 10 Pa) on chip samples from most of the samples using a magnetic balance (NMB-89, Natsuhara Giken, Osaka, Japan). In the measurements, chip samples were gradually heated from approximately 30°C to 700°C and then gently cooled to approximately 50°C, with the rate of 10°C/min. Throughout the temperature cycle, a field of 500 mT was kept applied to the sample.
To obtain unblocking temperature (TUB) spectra data for NRMs and isothermal remanent magnetizations (IRMs) both from the floor surface and the −20-cm level samples, each of two mini specimens from the samples 5 and 16 is subjected to thermal demagnetization (ThD) experiments. Because NRMs of the two samples were already demagnetized by AF of 20 mT in Nakajima et al. (1974), for a one set of the specimens, IRMs of 2.5 T were imparted by a pulse magnetizer (MMPM10, Magnetic Measurements, Lancashire, UK) and subsequently demagnetized at 20 mT using an AF demagnetizer (DEM-95, Natsuhara Giken). Stepwise ThD was then conducted on NRMs and IRMs of the mini specimens at 30°C to 50°C steps up to 600°C using a thermal demagnetizer (TDS-1, Natsuhara Giken). Remanent magnetizations were measured by a spinner magnetometer (ASPIN-A, Natsuhara Giken).
Scanning electron microscope (SEM) observation
Sliced pieces from the samples 5 and 16 were impregnated with epoxy and subsequently polished to mirror gloss. The polished surface of the pieces was then thin-coated with platinum and they were observed by a field emission scanning electron microscope (FE-SEM, JSM-6500F, JEOL Ltd., Akishimashi, Tokyo, Japan). We took backscattered electron images (BEIs) and made point analyses based on an energy-dispersive X-ray spectroscopy (EDS). Spatial resolution was as good as 10 to 100 nm in a BEI whereas it was a few micrometers at best for an EDS point analysis.
Tsunakawa-Shaw paleointensity experiments
The Tsunakawa-Shaw method (Tsunakawa and Shaw 1994; Yamamoto et al. 2003) was applied to mini specimens from all the samples to determine archeointensities (absolute paleointensities). This method estimates archeointensities based on coercivity spectra rather than blocking temperature spectra. Detailed procedures are described in Yamamoto and Tsunakawa (2005).
A specimen undergoes low-temperature demagnetization (LTD; Ozima et al. 1964). NRM after LTD is subjected to stepwise AF demagnetization. The remanence is measured at each step [NRM].
Anhysteretic remanent magnetization (ARM) is imparted to the specimen. Then, the specimen undergoes LTD. ARM after LTD is subjected to stepwise AF demagnetization and is measured at each step [ARM0].
The specimen is heated in a furnace to impart full TRM for the first time. Then, the same procedures as (i) and (ii) are performed for the TRM [TRM1] and ARM [ARM1].
The specimen is heated in the furnace to impart TRM for the second time. The same procedures as (i) and (ii) are performed for the TRM [TRM2] and ARM [ARM2].
For the remanent magnetization measurements, stepwise AF demagnetizations, and the impartment of ARMs, we used an automated spinner magnetometer with an AF demagnetizer (DSPIN, Natsuhara Giken). The demagnetizations were conducted up to 180 mT, with the steps at 2-mT intervals up to 30 mT, at 5-mT intervals up to 100 mT, and 10-mT intervals up to 180 mT. ARMs were imparted using a DC bias field of 50 μT with a peak AF of 180 mT, by setting the bias field direction approximately parallel to the NRM and laboratory TRM directions. LTD was conducted such that specimens were soaked in liquid nitrogen for 10 min and subsequently left at room temperature for 30 min in a zero field. For the impartment of TRMs, we used a thermal demagnetizer equipped with a DC field coil (TDS-1, Natsuhara Giken). The specimens were heated to 610°C in a vacuum (1 to 10 Pa) with the hold time of 10 (TRM1) and 20 (TRM2) min at that temperature and subsequently cooled down to room temperature for approximately 2 h in a 40-μT DC field throughout this process.
A primary component is resolved from NRM by stepwise AF demagnetization.
A single linear segment is recognized in the NRM-TRM1* diagram within the coercivity range of the primary NRM component. The segment spans at least 30% of the total extrapolated NRM (f N ≥ 0.30; definition of the extrapolation is the same as in Coe et al. (1978)). The correlation coefficient of the segment is not smaller than 0.995 (r N > = 0.995).
A single linear segment (f T ≥ 0.30 and r T ≥ 0.995) is also recognized in the TRM1-TRM2* diagram. The slope of the segment is unity within experimental errors (1.05 ≥ slopeT ≥ 0.95) as proof of the validity of the ARM correction.
For approximate estimations of remanence anisotropies of the samples, ARMs were imparted on unheated sister specimens with two different directions and those after LTD were measured. One direction was approximately parallel to the NRM direction (ARMNRM direction), and the other direction was to the laboratory TRM direction (ARMTRM direction). Conditions of the impartments were same as those in the main experiment.
Rock magnetic experiments
Results of the rock magnetic experiments and the Tsunakawa-Shaw paleointensity experiments
B rc /B c
M rs /M s
[10 -5 Am 2 /kg]
Scanning electron microscope (SEM) observation
Tsunakawa-Shaw paleointensity experiments
Only one successful result was obtained from the −20-cm level samples by the selection criteria. It yielded an archeointensity of 31.6 μT (Figure 8b and Table 1), which is inconsistent with the in situ geomagnetic field of 46.4 μT. In this result, the archeointensity is estimated from 74% of the total extrapolated NRMs (f N = 0.743) and degree of alteration in first laboratory heating is suggested to be negligible (slopeA1, = 1.01). Quality of this result seems to be also good in spite of the inconsistency.
On average, LTD demagnetized 21.4% and 10.0% of ARM0s for the floor surface and −20-cm level samples, respectively (Table 1). Because LTD treatment is known to be effective technique for selective removal of MD-like remanences in Ti-poor titanomagnetite (Ozima et al. 1964; Dunlop and Ozdemir 2007), it is considered that these samples certainly had such remanences but they are more or less removed.
About the remanence anisotropies of the samples, ratios of ARMTRM direction to ARMNRM direction resulted in 0.941 to 1.12 except for the sample 12 which showed the ratio as 1.24 (Table 1). These values seem to be typical of baked clays, for example, Kovacheva et al. (2009) reported that baked clay and soils collected from archeological sites in France and Bulgaria resulted in TRM anisotropy ratios less than 1.20 for about 80% of the collection.
From the in situ temperature record during the firing (Figure 2), it is clear that the floor surface samples experienced high temperature of approximately 1,000°C while the −20-cm level samples were only exposed at low temperature, at most approximately 350°C. It is considered that the former samples were baked well above the Curie temperature of magnetite (approximately 580°C) resulting in acquisition of full TRMs, whereas the latter ones were below that temperature leading to acquisition of partial TRMs. The acquisition of full and partial TRMs for the former and latter samples are respectively implied from the results of the ThD experiments (Figure 6). In the Tsunakawa-Shaw experiment, we imparted full TRMs to the samples in laboratory and basically compared them with their NRMs. For the floor surface samples, NRMs are probably full TRMs and the comparison seem to result in the accurate archeointensities. In contrast, for the −20-cm level samples, NRMs are probably weak partial TRMs and thus the comparison would probably result in the weak paleointensity.
Difference in the ‘baking’ temperatures between the floor surface samples and the −20-cm level samples would probably also cause the differences in the rock magnetic characters. In the former samples, there are much more SD and/or SP titanomagnetite grains compared with the latter samples, and the former samples have high remanence intensities (e.g., ARM0s). From the view of the rock magnetic properties, the floor surface samples seem to be much more preferable for high-fidelity archeointensity researches.
Importance of the anisotropy correction has been emphasized for accurate archeointensity determinations (e.g., Aitken et al. 1981). The Tsunakawa-Shaw method employs a built-in anisotropy correction using ARMs: ARM0, ARM1, and ARM2 are imparted with their directions approximately parallel to the NRM, TRM1, and TRM2 directions, respectively, and measured along with the stepwise AF demagnetizations; ratios of ARM0/ARM1 and ARM1/ARM2 are used to correct TRM1 and TRM2 into TRM1* and TRM2*, respectively. The floor surface samples yielded the successful archeointensity results fairy consistent with the in situ geomagnetic field, and thus the built-in correction seemed to work well. The degree of the correction is suggested to be 6% to 12% except for sample 12 considering the ratios of ARMTRM direction to ARMNRM direction (Table 1).
Necessity of the cooling rate correction has also been emphasized in many studies because the difference in that rate could result in biased archeointensity estimates (e.g., Mitra et al. 2013; Cai et al. 2014). For example, Usui (2013) reported that the cooling rate effect resulted in a 37% to 46% overestimated paleointensity for an oceanic gabbro, although it is not the case of the archeointensities. In the present study, there is large difference in the cooling rates between the kiln NRMs (approximately 24 h) and the laboratory TRMs (approximately 2 h). However, without such corrections, we obtained the archeointensity results fairy consistent with the in situ geomagnetic field from the floor surface samples. This suggests that the cooling rate correction is dispensable for the Tsunakawa-Shaw method, at least for a baked clay. It is noted that the main magnetic carriers of the floor surface samples might be Ti-poor titanomagnetites in fine PSD sizes, rather than in approximately 10 nm size: Yu (2011) experimentally demonstrated that the cooling rate effect was negligible for a 1.06 μm PSD magnetite.
Application of the Tsunakawa-Shaw method to the baked clay samples taken from a reconstructed kiln shows that the samples from floor surface provide the accurate archeointensity results. They are obtained with a built-in anisotropy correction using ARM and without any cooling rate corrections. A suite of the rock magnetic experiments and the SEM observations elucidate that dominant magnetic carriers of the floor surface samples are Ti-poor titanomagnetite grains in approximately 10 nm size, with SD and/or SP states. For archeointensity researches, baked clay samples from a kiln floor are considered to be ideal materials.
We thank Tadashi Nakajima and Katsumi Yaskawa for the reconstruction experiment, Kimio Hirooka and Hiroshi Nakamura for long-term storage of the samples, and Yukako Nabeshima for help with the measurements. Constructive comments by Yongjae Yu and Hidetoshi Shibuya improved the manuscript. This study was partly supported by JSPS KAKENHI Grant Numbers 21500991, 23740340, and 25247073 and by the Kochi University Research Project ‘Research Center for Global Environmental Change by Earth Drilling Sciences.’
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