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Paleomagnetic study of basaltic rocks from Baengnyeong Island, Korea: efficiency of the Tsunakawa–Shaw paleointensity determination on non-SD-bearing materials and implication for the early Pliocene geomagnetic field intensity
Earth, Planets and Space volume 71, Article number: 126 (2019)
Finding the statistical intensity signatures of the Earth’s magnetic field over geologic time has helped understanding of the evolution of the Earth’s interior and its interactions with other integral parts of Earth systems. However, this has been often hampered by a paucity of absolute paleointensity (API) data, which are difficult to obtain primarily because of non-ideal magnetic behaviors of natural materials. Here, we present new API determination data with paleodirectional and rock magnetic analyses from basaltic rocks probably aged ~ 4‒5 Ma in Baengnyeong Island, Korea. Paleodirectional analysis obtained an overall mean direction of D = 347.3° and I = 38.3° (α95 = 4.9°, k = 113.4) corresponding to a virtual geomagnetic pole at 342.1° E and 70.2° N. Comprehensive rock magnetic analyses identified Ti-poor titanomagnetite with, in part, multi-domain (MD) particles as a main carrier of remanent magnetization. The Tsunakawa–Shaw (TS) method yielded 12 qualified API estimates with a high success rate, efficiently removing possible MD influences, and resulted in a mean value of 13.1 μT with good precision (1.7 μT, standard deviation). The Thellier method of the IZZI protocol with pTRM checks, coupled with the use of a bootstrap approach instead of the “conventional best-fitting” in API determination, gave 6.6‒19.7 μT as a 95% confidence interval of its mean API estimate, which supports the reliability of our TS-derived API mean estimate; but it is not considered in the final mean value because of the relatively large uncertainty. The virtual dipole moment corresponding to the TS-derived API mean, 2.9 (± 0.4) × 1022 Am2, is somewhat lower than the expectations of the past few Myr averages. Combined with a global API database, our new data implies a larger dispersion in the dipole moment during the early Pliocene than previously inferred. This also suggests that the issue of whether the early Pliocene average dipole strength was moderately high (> 5 × 1022 Am2) or consistent (4‒5 × 1022 Am2) should be discussed further.
The history of Earth can be investigated by seeking its magnetic field evolution, which is associated with the evolution of its deep interior (Gubbins and Richards 1986; Gubbins 1988; Glatzmaier et al. 1999; Roberts and Glatzmaier 2000; Costin and Buffett 2004; Biggin et al. 2015; Tarduno et al. 2015) but may also interact with other integral parts of the Earth system on variable geological time scales (Courtillot et al. 2007; Tarduno et al. 2007; Lee and Kodama 2009; Tarduno et al. 2010; Kitaba et al. 2012, 2017). For a complete picture of the geomagnetic field over time, it is clearly useful to acquire directions and intensities of the surface paleomagnetic field from geological materials (paleomagnetic full-vector data).
However, geological and experimental alterations of materials often create non-ideal magnetic properties as less suitable magnetic recorders, which often prohibits estimation of such paleofield directions and intensities. This has led, to date, to a sparsity (in terms of geological time and space) of reliable paleomagnetic data, of highly variable quantity and quality, over. In particular, such a limitation is more conspicuous in absolute paleointensity (API) data, which often leads to inconsistent views about the time-averaged statistical signature of the geomagnetic field on million year (Myr) timescales and its temporal evolution (e.g. McFadden and McElhinny 1982; Goguitchaichvili et al. 1999 versus Juarez and Tauxe 2000; Cromwell et al. 2015 for the past few Myr). Despite the significant effort by many paleomagnetists over the world, the temporal coverage of API data is concentrated into the past few Myr, dropping sharply at ~ 4 million years ago (Ma) and for older periods. In East Asia, particularly, the paucity of data becomes evident for time periods older than ~ 1 Ma. In the case of PINT (version 2015.05; http://earth.liv.ac.uk/pint/, accessed July, 2018; see Biggin and Paterson (2014)), a global API database, the number of API data (NAPI) for the past 4 Myr is 1730 (40%) out of 4293 with data populations of 144‒1059 per 1 Myr (/Myr), which is much higher compared than the < 100/Myr in the other older periods, and in East Asia (100‒150° E; NAPI = 387, 9% of the total) the data populations for the past 1 Myr and the other order periods are 138/Myr and < 55/Myr, respectively.
Recently, a number of API studies (Yamamoto and Tsunakawa 2005; Ziegler et al. 2011; Cromwell et al. 2015; Wang et al. 2015) have found that the axial dipole moments of the geomagnetic field during periods of the Plio‒Pleistocene, on average, were approximately 4‒5 × 1022 Am2. Furthermore, integrating results from some previous studies (Goguitchaichvili et al. 2003; Pan et al. 2005; Lhuillier et al. 2019) could suggest that a moderately high state of the dipole strength, at least as high as ~ 6 × 1022 Am2, lasted for an approximately long geologic period from the Middle‒Late Miocene (~ 10 Myr length). However, due to the paucity of qualified API data, how long-term field structures change between the Late Miocene and the Pliocene remains unclear.
In fact, the determination of API is much more difficult and time-consuming than determining field direction. Researchers have developed a variety of methods for API determination with different theoretical/experimental protocols and conditions, and material types and sizes. These are mostly targeting API determinations in blocking temperature (Tb) space. For bulk rock samples, the Thellier-type methods have been classically the most frequently utilized with various experimental conditions and protocols (Thellier and Thellier 1959; Coe 1967; Aitken et al. 1988; Riisager and Riisager 2001; Tauxe and Staudigel 2004; Wang and Kent 2013); however, they are prone to high failure rates for API determination due to non-ideal behaviors in the experiments, such as sagged (or curved or concave-up), kinked, zigzagged, and S-shaped patterns in the Arai diagram (Nagata et al. 1963; the plot of natural remanent magnetization (NRM) remaining versus laboratory-induced thermoremanent magnetization (TRM) gained).
Generally, ideal materials for API determination are rare in nature. Thus, a number of additional experimental protocols have been suggested: the “pTRM check” (where pTRM denotes partial TRM; Prévot et al. 1985), the “pTRM-tail check” (Riisager and Riisager 2001), the “IZZI protocol” (Tauxe and Staudigel 2004; Yu et al. 2004) for detecting and rejecting non-ideal results, and the second API experiment that uses a lab simulated NRM proposed by Wang and Kent (2013) for correcting non-ideal results arising from multi-domain (MD) magnetic particles. The additional protocols have enhanced the number of reliable API data, but there is still a limitation; whichever of the above protocols are used, it is still time-consuming and subject to moderate rates of acquisition of reliable API determinations. As a different approach, Bowles et al. (2005) and Shaar et al. (2011) utilized a new bootstrap procedure instead of the conventional best-fitting line procedure for determining an API estimate in MD-like curved Arai plots; it is based on the observation that two “end-case” slopes in the curved Arai diagram can provide adequate constraints for the true API value. It has the potential to enhance the acquisition rate of meaningful API values with Thellier-based methods, although interpretation should be careful.
An alternative promising technique is to obtain API data in coercivity (Hc) space: one of such techniques with a high success rate even from non-ideal materials is the Tsunakawa–Shaw method (Tsunakawa and Shaw 1994; Yamamoto et al. 2003; Mochizuki et al. 2004; Oishi et al. 2005; also called “LTD-DHT Shaw method”). This technique is the most advanced variant of the Shaw method (Shaw 1974) coupled with ARM correction, low-temperature demagnetization (LTD) treatment, and a double heating test (DHT). It can detect and even correct for non-ideal behaviors in the associated results and generate a qualified API estimate by the following procedure: selective demagnetization of MD-like remanence by the LTD treatment (Yamamoto et al. 2003), correction for laboratory thermal alteration by anhysteretic remanent magnetization (ARM) (Rolph and Shaw 1985), and checking the validity of the ARM correction by DHT (Tsunakawa and Shaw 1994). Successful applications of the method have been validated in historical lava flows in Japan and Hawaii (Yamamoto et al. 2003; Mochizuki et al. 2004; Oishi et al. 2005; Yamamoto and Hoshi 2008). Furthermore, for old volcanic rocks and burnt archeological materials, the method has yielded indistinguishable API estimates from those obtained by the Thellier-type methods (Yamamoto et al. 2010; Ahn et al. 2016; Kitahara et al. 2018; Yamamoto and Yamaoka 2018).
In this study, we report new API data from early Pliocene volcanic units (“Jinchon Basalt”, ~ 4‒5 Ma) in Baengnyeong Island, Korea, to fill the gap in the current global API database. Analyzed samples, containing MD magnetic minerals, are taken from two units of the same age (statistically indistinguishable from each other). We apply not only the Tsunakawa–Shaw method (hereafter referred to as the ‘TS method’) but also the Thellier method of the IZZI protocol (hereafter referred to as the ‘IZZI-T’ method) with pTRM checks. An additional use of a bootstrap approach in API determination is adapted to a result obtained by the IZZI-T method to compare with and examine the TS determination. Combining the API results by the TS method and the IZZI—T method, we can have a robust API estimate in the early Pliocene.
Brief geological background and samples
Late Cenozoic alkali magmatism in East Asia is known to originate in the shallow asthenosphere, largely in response to dramatic changes in stress regimes, which resulted from the interplay between the India-Eurasia collision and subduction of the Pacific Plate beneath the eastern margin of Eurasia (Choi et al. 2006). The associated basaltic rocks, with estimated ages in the Mio-Pliocene, are sparsely distributed in South Korea (Fig. 1a) and include Baengnyeong Island (~ 4–7 Ma; Kim et al. 2005; Choi et al. 2006), the Goseong area (~ 6–7 Ma; Choi et al. 2006), Pyeongtaek-Asan area (~ 14–19 Ma; Shin et al. 2006), Boun area (~ 11 Ma; Arai et al. 2001), and Ulsan-Gyeongju area (~ 16–22 Ma; Jin et al. 1988). Many outcrops of these Mio-Pliocene basaltic rocks still need more accurate and precise geochronological constraints.
Baengnyeong Island (37° 55′ N, 124° 40′ E) is 45 km2 in area and is situated off the furthest northwest point of South Korea (Fig. 1a). Part of the tectonic regime of the Korean Peninsula, the island lies within the Phanerozoic Imjingang Belt, which is in contact with the Precambrian Gyeonggi Massif (or Gyeonggi Block) to the south and the Precambrian Nangrim Massif (or Nangrim Block) to the north and has been considered the eastern extension of the collision zone between the North China Block and the South China Block (or between the North Sino-Korea Block and the South Sino-Korea Block) (Chough et al. 2000). Figure 1b shows a simplified geological map of Baengnyeong Island (modified from Park and Park 1996; Lim et al. 1999). The oldest strata of the island, which are the majority, are composed of Proterozoic metasedimentary rocks (slate, phyllite, and quartzite). The Proterozoic strata are intruded by dioritic dikes of unknown age (presumably Late Cretaceous to Paleogene). The middle part of the island is covered by Quaternary alluvium and beach sand layers. In the northeastern part of the island, Neogene intrusive and extrusive volcanic rocks are exposed covering ~ 4 km2, called Jinchon Basalt, which have been previously reported to have a variety of compositions, including alkali basalt, trachybasalt, basanite, and phonotephrite in Park and Park (1996) and Choi et al. (2006), and even basaltic andesite and basaltic trachyandesite in Kim et al. (2002). The Jinchon Basalt rocks contain mantle-derived spinel peridotite xenoliths (Park and Park 1996; Choi and Kwon 2005; Choi et al. 2005). For the host rocks there are documentations of whole-rock K–Ar ages: 4.2 ± 0.1 (1σ) Ma for basanite (Choi et al. 2006), 6.4 ± 0.2 (1σ) Ma for phonotephrite, and 7.1 ± 0.3 (1σ) Ma for basaltic andesite (Kim et al. 2005).
For two Jinchon Basalt rock sites named B1 and B2 along the coast of the exposures, 7 oriented block samples each were collected in 2007 (collectively 14 block samples). The distance between these two sites is ~ 0.3 km. Relationship between the two exposures (e.g. the same versus different cooling units?) remained uncertain in the field observation due to the discontinuity spacing of the exposures. The sampled sites were regarded as the same place, or very close, to where the K–Ar age of ~ 4.2 Ma was assigned by Choi et al. (2006). It is also said to be ~ 5 Ma or so for the age of the exposures by unpublished radiometric age data (personal communication with Dr. Youn Soo Lee of Pohang University of Science and Technology). Considering the uncertainty of age determination for now, we thus assign ~ 4–5 Ma as a tentative age of our sampled rocks. The orientation was made using a magnetic compass equipped with a tripod. A lack of bias to the needle of the magnetic compass influenced by the basalt outcrops was confirmed by monitoring the declination changes of the compass needle while moving in lines perpendicular to the outcrop planes. At the laboratory of the Center for Advanced Marine Core Research (CMCR), Kochi University, Japan, multiple cylindrical specimens 25 mm in diameter and ~ 12‒22 mm in height were prepared from each of the collected samples. For these specimens, name of a specimen consists of site name, block sample code, and core and specimen (sub-core) numbers (for example, specimen B1A-1-1 means that he site name is B1, the block sample code is A, and the following 1-1 is core and specimen numbers). In addition, multiple small fragments (tiny subsamples), a few tens of mg in weight, were selectively prepared from each of the drilled long cylindrical subsamples. Naming of these fragment specimens are similar as the above case for the cylindrical specimens (but, sometime, the specimen number was used to be omitted in the specimen name; see Fig. 2a–c).
Rock magnetic and paleomagnetic experiments conducted in this study were conducted at the CMCR laboratory of Kochi University.
Measurements of rock magnetic properties
Using a MPMS-XL5 magnetic property measurement system (Quantum Design), remanence measurements at low temperatures were performed on powdered subsamples prepared from the small fragments with two different experimental sequences: (1) thermal demagnetization during zero-field warming (ZFW) of an isothermal remanence (IRM) imparted with a 2.5 T field at 10 K after zero-field cooling (ZFC) from 300 K (ZFC remanence) and (2) thermal demagnetization during ZFW of a remanence taken during cooling from 300 to 10 K with a field of 2.5 T (FC remanence). Additionally, the temperature dependence of low-field magnetic susceptibility was measured at 1, 10, 100, and 1000 Hz.
Using an NMB-89 magnetic balance (Natsuhara Giken), a small fragment of each sample was subjected to high-temperature thermomagnetic analyses, where it was heated from the room temperature (~ 20 °C) to 700 °C and then cooled to 50 °C, in a constant applied field of 0.5 T and an average heat rate of ~ 10 °C/min, under the ambient air environment.
Using a MicroMag 3900 vibrating sample magnetometer (VSM; Princeton Measurements Corporation), a magnetic hysteresis loop and determinations of hysteresis parameters (saturation magnetization, Ms; saturation remanent magnetization, Mrs; coercive force, Bc; and coercivity of remanence, Bcr) were each made on a chip subsample, with a maximum applied field of 0.5 T. Then, with the VSM, 263 first-order reversal curves (FORCs) were also measured at an averaging time of 100 ms applying a maximum applied field of 1 T. The FORCs were analyzed with the FORCinel software (Harrison and Feinberg 2008) and the results displayed on a FORC diagram.
Paleomagnetic direction analyses
A suite of NRM measurements and alternating field (AF) demagnetizations were performed on prepared cylindrical specimens using a DSPIN automated spinner magnetometer equipped with an AF demagnetizer (Natsuhara Giken). Prior to the AF procedure, each specimen was subjected to LTD treatment, in which the specimen was placed in a dewar bottle filled with liquid nitrogen and the assemblage kept in a Mu-metal shield space (near-zero-field) for 10 min and then left at the room temperature for approximately 30 min in the zero field. The AF demagnetizations (AFDs) were set to 34 steps in peak fields from 2 to 140 mT. These 11 LTD-AFD-treated specimens were afterwards used in the Tsunakawa–Shaw PI experiments. For directional analyses, compass readings of the sample orientation were corrected for the site declination of the present-day Earth’s magnetic field of − 8°. The progressive demagnetization data for each specimen were identified with the orthogonal vector diagram of Zijderveld (1967) and equal-area projection. To determine particular directions of remanent magnetizations for each specimen-level demagnetization data, principal component analysis (PCA) was performed applying the Kirschvink method (1980). If necessary, the great-circle-fit technique (Kirschvink 1980) was also used for direction determination. Mean directions for the determined remanence components were calculated using Fisherian statistics (Fisher 1953).
Tsunakawa–Shaw (TS) method
For 21 prepared cylindrical specimens from the two sites, the TS API experiments were conducted following a procedure similar to the one described in Yamamoto and Tsunakawa (2005). Remanence measurements, AFD treatments, and acquisitions of anhysteretic remanent magnetization (ARM) were made using the DSPIN automated system. AFD treatments all were performed with 34 (or 38) steps in the peak AFs from 2 to 140 (or 180) mT. All ARMs were imparted by a direct current (DC) bias field of 50 mT with the peak AFs of 180 mT, in which the bias field directions were (sub-)parallel to the characteristic directions of NRM or laboratory-induced TRM directions. In acquiring the laboratory TRMs the specimens were heated to 610 °C in a vacuum (1‒10 Pa), held at that temperature for 45 (for the first TRM acquisition, TRM1) and 60 min (for the second TRM acquisition, TRM2), and then cooled to the room temperature for ~ 3 h, using a TDS-1 thermal demagnetizer with a built-in DC field coil (Natsuhara Giken). The set DC field was variable between 15 and 30 μT. Before starting progressive AFD treatment of remanent magnetization, LTD was conducted as described in “Paleomagnetic direction analyses” section.
The experimental result for each specimen was plotted on NRM versus TRM1* and TRM1 versus TRM2* diagrams, where TRM1* and TRM2* are the corrected TRMs using the ARM correction technique of Rolph and Shaw (1985) in the first and second heating, respectively, expressed as TRM1* = TRM1 × ARM0/ARM1 and TRM2* = TRM2 × ARM1/ARM2, where TRM1, TRM2, ARM0, ARM1, and ARM2 are the remanence intensities at each AF step.
An API value was estimated by determining the slope of the linear segment defined for the NRM-TRM1* diagram when the ARM correction was validated by the slope of unity of the linear segment of the TRM1–TRM2* diagram. Each API estimate was judged by a set of the following selection criteria, which are similar to those adopted in the recent TS-based paleointensity studies (Yamamoto et al. 2010, 2015; Yamazaki and Yamamoto 2014; Ahn et al. 2016):
A primary NRM component should be isolated by progressive AFD on the Zijderveld diagram.
On the NRM-ARM1* diagram, a single linear segment for the slope calculation should be recognized within the coercivity range defining the primary NRM component. The segment should have at least 30% of the total extrapolated NRM intensity [fN ≥ 0.30, where the definition of fN is equivalent to that designed by Coe et al. (1978)]. Its correlation coefficient should not be less than 0.995 (rN ≥ 0.995).
On the TRM1-TRM2* diagram, a single linear segment should also be recognized with fT ≥ 0.30 and rT ≥ 0.995. Its slope is unity within experimental errors with 1.05 ≥ slopeT ≥ 0.95, as proof of the validity of the ARM correction.
IZZI-Thellier (IZZI-T) method with pTRM checks
For eight selective cylindrical specimens (six for site B1 and 2 specimens for site B2), the IZZI-T PI experiments with pTRM checks were performed. The peak temperatures of heating steps set in this study were, in addition to the room temperature, 150, 225, 300, 335, 370, 400, 435, 470, 500, 520 (or 525), 545 (or 550), 570 (or 575), and 600 °C. All heating–cooling procedures were performed in air using a TDS-1 thermal demagnetizer equipped with a built-in fan (Natsuhara Giken). Remanence measurements were made using a SMD-88 spinner magnetometer (Natsuhara Giken) at the room temperature and after every heating–cooling treatment. At each temperature step, the specimen was heated to that temperature, maintained for 25 min, and then cooled to the room temperature using the built-in fan, both in the presence (in-field step) and absence (zero-field step) of a laboratory field (Flab = 15 μT, which was directed along the y-axis (+ y) of the specimen, for this study). Note that the laboratory field, 15 μT, is for minimizing the difference in intensity with the field in which the NRM was acquired, based on the TS results later described in “API determination” section, because of the adverse effect on the Arai diagram as found by Shaar et al. (2011). The order of in-field and zero-field steps was alternated at each temperature step [in-field-zero-field (IZ) versus zero-field-in-field (ZI)]. The pTRM check steps were inserted between every ZI step.
Each specimen-level experimental result was analyzed in the Arai diagram using the Thellier GUI program included in the PmagPy software package (Shaar and Tauxe 2013; Tauxe et al. 2016). To evaluate API determination on each specimen-level result using the conventional best-fitting line procedure, we used the following statistics: n, npTRM, DRATS, SCAT, FRAC, Gap Max, Beta (β), MADfree, DANG, k′. Definitions of each statistic can be found in Paterson et al. (2014) as well as Cromwell et al. (2015), and brief descriptions of these statistics are as follows:
n: the number of points on an Arai diagram used to estimate the best-fit linear segment (the PI),
npTRM: the number of pTRM checks used to estimate the best-fit segment on an Arai diagram,
DRATS (Tauxe and Staudigel 2004): the sum of the difference between the original pTRM at a given temperature step and the pTRM check, normalized by the pTRM gained at the maximum temperature used for the best-fit on the Arai diagram,
SCAT (Shaar and Tauxe 2013): a Boolean statistic that uses the error on the best-fit Arai diagram slope to test the degree of scatter over a range of NRM/TRM data points,
FRAC (Shaar and Tauxe 2013): a measure of the NRM fraction of a selected range of NRM/TRM data points on an Arai diagram, based on the vector difference sum calculation,
Gap Max (Shaar and Tauxe 2013): the maximum gap between two NRM/TRM data points determined by vector arithmetic,
Beta (β) (Coe et al. 1978; Tauxe and Staudigel 2004): a measure of the relative scatter around the best-fit line in an Arai diagram,
MADfree (Kirschvink 1980): maximum angular deviation of the free-floating directional fits to the paleomagnetic vector in selected NRM steps on a vector component diagram,
DANG (Tanaka and Kobayashi 2003; Tauxe and Staudigel 2004): the angular difference between the free-floating best-fit vector and the direction passing by the data center of a mass and the origin for selected NRM data points on a vector component diagram,
k′ (Paterson 2011; Paterson et al. 2015): a measure of the degree of curvature between a selected range of the data points in an Arai diagram.
Our bundle of the statistics were mainly based on those documented by Cromwell et al. (2015), and adopted their threshold values as a selection criteria for evaluation (the so-called CCRIT selection criteria) with minor modifications that involve threshold values of three additional statistics, n and npTRM, and DRATS (as its threshold value, adopted that in Donadini et al. 2011; Sprain et al. 2016, etc.) that replace SCAT (not used in evaluating our API results). Our adopted threshold values of the statistics are as described below:
n ≥ 4, npTRM ≥ 2, FRAC ≥ 0.78, Gap Max ≤ 0.60, β ≤ 0.10, MADfree ≤ 5.0°, DANG ≤ 10.0°, |k′| ≤ 0.164, and DRATS ≤ 22.0°.
Results and discussion
Rock magnetic signature
Representative results of rock magnetic measurements are summarized in Fig. 2.
Figure 2a shows results of the in-air high-temperature thermomagnetic curves on representative subsamples. The curves are slightly different between sites but share a common characteristic that has a Curie temperature (Tc) between 560 and 570 °C during the heating curve and reduction in magnetization intensity at the cooling curve after heating. This is suggestive of the presence of nearly pure magnetite or Ti-poor titanomagnetite (presumably x < 0.1 for the Fe3-xTixO4 formula) in the natural samples and possible occurrence of oxidation of (titano-)magnetite to (titano-)hematite during the laboratory heating.
Low-temperature thermomagnetic curves of FC and ZFC remanences and of magnetic susceptibilities (m = m′ – i m″, where m′ and m″ are the in-phase magnetic susceptibility and the out-of-phase susceptibility, respectively) with different frequencies on a representative subsample, respectively, are shown in Fig. 2b, c. The curves of FC/ZFC remanence and susceptibility show, respectively, a broad but marked intensity transition at around 100‒120 K and a peak in m′ and minimum in m″ at ~ 110 K; this is considered to be related to the Verwey transition temperature for Ti-poor titanomagnetite (Özdemir et al. 1993; Moskowitz et al. 1998), existence of which is obviously supported by the Tc determined from the high-temperature curves. In addition, there also appears to be a transition in FC/ZFC remanence and a maximum in m″ at around 40‒50 K for both of the low-temperature thermomagnetometry. In this study the source of the ~ 40‒50 K transition cannot be well constrained. Several candidate magnetic minerals for the source are possible: a rhombohedral phase of Fe–Ti oxide (Ishikawa et al. 1985), an antiferromagnetic mineral such as ilmenite (Moskowitz et al. 1998), magnetite (Moskowitz et al. 1998; Skumryev et al. 1999), or partially oxidized magnetite (Özdemir et al. 1993). The former two candidates have no remanent magnetization at the room temperature.
Magnetic hysteresis parameters on an Mrs/Ms versus Bcr/Bc diagram (Day et al. 1977) and FORC analysis provide information about grain size and magnetic interactions of the contained magnetic minerals. Our hysteresis parameters data in the Day diagram lie on the SD-MD mixing curves (Fig. 2d). The observed FORC diagrams are represented by two intensity peaks around 20‒30 mT and near-zero mT on the Bc axis and some spreading of contours in the Bu-axis-direction (Fig. 2e). Furthermore, the slightly larger remanence intensity in FC than ZFC (Fig. 2b) is analogous to the FC/ZFC curves for sample 3006, which has a nominal grain size of 2‒3 µm corresponding to PSD sizes, documented in Kosterov (2003). These infer mixtures of magnetostatically interacting large SD (or PSD-like) and MD particles in our samples.
In addition, ratios of the hysteresis parameters Mrs/Ms and Bcr/Bc allow us to calculate the bulk domain stability (BDS), which is suggested by Paterson et al. (2017) and is a quantitative parameter representing the degree of capability in maintaining stable remanence, also associated with content of MD particles (see Paterson et al. (2017) for BDS calculation, where BDS value is 1 when a single grain yields a perfectly square hysteron). BDS values of our analyzed samples range between 0.12 and 0.52 (see Fig. 2d), where Paterson et al. (2017) described the BDS threshold of > 0.1 as a first-order threshold, aimed at screening out samples that will not be useful in the API experiments.
A total of 11 specimens for 2 sites were analyzed to isolate the characteristic remanent magnetization (ChRM) of each from progressive AF demagnetization with pre-LTD-treatment. All the specimens, except specimen B1D-2-1, revealed similar directions after demagnetization by ~ 10‒20 mT (see Fig. 3a). Specimen B1D-2-1 exhibited an anomalous direction in high demagnetization steps. This could arise from misorientation in specimen preparation. Through PCA, a stable ChRM direction was well defined with MADfree < 8° for each specimen, except for one (B2B-2-1), which exhibited a strong overprint of secondary remanence of reverse-magnetized. Hence, individual site-mean ChRM directions for the two sites could be calculated as listed in Table 1. These two site-mean directions are close to and statistically indistinguishable from each other, thereby allowing us to obtain an in situ overall mean of D = 347.3° and I = 38.3° with α95 = 4.9° and k = 113.4 (n = 9) (see also Fig. 3b).
The overall mean is obviously different from both the present field direction (D = ~ 352°, I = ~ 55°; IGRF-12, Thébault et al. 2015) and the expected geocentric axial dipole (GAD) direction at the studied geographic location (D = 0°, I = ~ 57°). The corresponding virtual geomagnetic pole (VGP) is at 342.1° in longitude and 70.2° in latitude (with dp = 3.4° and dm = 5.8°) (Fig. 3c), which is ~ 20° from both the geographic North Pole and the reference pole for East Asia at ~ 5 Ma from Cogné et al. (2013). These results probably originate from an instantaneous feature of the Jinchon Basalt: timing of the emplacement and cooling cannot be known exactly but is presumed as being geologically short, insufficient to average out the paleomagnetic secular variation during a period of normal polarity.
Tsunakawa–Shaw (TS) determination
For specimens subjected to the TS method, about 11‒24% of ARM0 intensity was demagnetized by LTD (see LTDA00 values in Table 2), suggestive of the relatively large contribution of the remanence component carried by MD particles.
Examples of the TS API results for two specimens (B1A-1-1 and B2C-1-1) meeting our set of criteria (see “Tsunakawa–Shaw (TS) method” section) are shown in Fig. 4a. In each of the NRM-TRM1* diagrams a linear segment cloud be defined after AF demagnetizations by 8‒22 mT (soft), in which the MD-carried remanence component could be erased. The individual determined linear segment has a large portion (fN > 0.7) and high value in the correlation coefficients (rN ≥ 0.998).
Non-ideal results that could not meet the specimen-level selection criteria, such as in Fig. 4b (an example of specimen B2B-1-1), all fail by reason of low correlation coefficient values in the NRM-TRM1* diagrams (rN < 0.995) and non-unity of the slope in the TRM1-TRM2* diagrams (slopeT > 1.05). It is also found that these failed results have a large portion of unusual overprint of remanence in low-coercivity spectra on the individual orthogonal diagrams of the NRM demagnetization result.
The TS experiments yield 13 (out of 21) specimen-level API estimates that meet our set of criteria (Table 2). The acquisition rate of the acceptable API estimates is 62%. All of the specimen-level acceptable estimates, with one exception (specimen B2F-1-1, 3.3 μT), yield values in range between 11.3 and 15.9 μT, which represent remarkably low values compared to the present-day intensity at the site location (~ 52 µT). These allow two mean API values, 12.6 μT (± 1.2 μT, standard deviation; N = 10) and 15.9 μT (± 0.1 μT; N = 2 when discarding the B2F-1-1 estimate in calculation) for the B1 and B2 site, respectively (Table 2). Since, despite of the somewhat difference of site means between them, both indicates low estimates, we combine the 12 specimen-level estimates of both sites, excluding the B2F-1-1 estimate (3.3 μT), and obtain an overall mean of 13.1 μT with a standard deviation of 1.7 μT (13% of the mean).
We also obtain similar API estimates from all pairs of companion specimens that were set to different Blab values in the experimental condition (see Table 2). It is also found that there is a consistency in the API estimates even for samples with variability in the average size of contained magnetic particles (for example, the BDS values ranging from ~ 0.3 to ~ 0.5 as shown in Fig. 2d). The independence of the API estimates from both the Blab value and the magnetic stability suggests high-fidelity API estimates by the TS method.
IZZI-Thellier (IZZI-T) determination
Eight specimens from six samples (five for B1 site and one for B2 site) were subjected to the IZZI-T API experiments. Examples of the IZZI-T results are shown in Fig. 5. NRM/TRM data points in the Arai diagram appear to fall onto a curved or kinked line, leading to a failure to determine a characteristic straight line in which the slope was utilized in the API calculation. All the Arai diagrams analyzed reveal such problematic patterns for API determination; this is not surprising because there are certainly contributions from MD remanences in the samples, as suggested from the LT-demagnetized components in ARMs and the FORC diagrams. The degree of the curvature vary by sample (the k values given in Table 3). NRM directions for the zero-field steps appear to be similar after 225 °C but the direction becomes closer to the laboratory field directions as the temperature step increases. These characteristic observations are likely to be responsible for the effect of the MD particles. The pTRM checks are still positive at 500 °C or higher, although the pTRM check at 550 °C appears to be inconclusive or negative.
Due to their curved signature patterns, each of the analyzed Arai diagrams can take variable slope values corresponding to (not actual) API estimates spanning mostly from ~ 3 to > 30 μT. Examples of API determinations by the conventional best-fitting line technique for the individual diagrams are given in Table 3. In all analyzed specimens, there are no API determinations meeting our criteria. Thus, it is concluded that the best-fitting line technique for our IZZI-T results cannot give meaningful API estimates.
The cause of the curved (or two-slope) Arai diagrams is hard to be clarified in this study but it is possibly considered to be dominantly related to the presence of MD particles (see, e.g. Levi 1977; Fabian 2001; Coe et al. 2004; Leonhardt et al. 2004; Xu and Dunlop 2004; Shaar et al. 2011; Paterson et al. 2015), which was suggested by the results of the hysteresis parameters and FORC diagrams (as documented in “Rock magnetic signature” section) and the intensity decay of remanences by LTD (see “Tsunakawa–Shaw (TS) determination” section). The occurrence of MD particles can be also supported by the “zigzagged” pattern, being superimposed on the curved Arai diagram, as seen in Fig. 5 (Tauxe and Staudigel 2004; Yu et al. 2004; Yu and Tauxe 2005). On the other hand, considering the rock magnetic signatures of the samples in more, magnetic interaction between the particles (e.g. Mankinen and Champion 1993) and/or thermal alteration of pre-existing magnetic minerals during the experiment (e.g. Mochizuki et al. 2004) might be also another possible cause for them. However, the magnetic interactions seem to be not the case for this as Coe 1974 and Fabian 2001 found that an average magnetostatic interaction of the particles is not likely to influence the shape of the Arai diagram noticeably. Mochizuki et al. (2004) reported, for PSD-like Ti-poor and Ti–rich titanomagnetites-bearing samples of the Oshima 1986 lava, two-slope Arai patterns on the Coe’s version Thellier experiments (Coe 1967) and change in the remanence directions at the zero-field steps converging towards the direction of the lab field above elevated temperatures. They attributed them to acquisition of chemical remanences by gradual thermal alteration of the contained magnetic minerals with intermediate degrees of high-temperature oxidation due to the laboratory heating during experiment. We consider this to be not the case for our Thellier results because our samples do not contain such Ti-rich titanomagnetites thereby being hard to follow the scenario possibility of the magneto-mineral change Mochizuki et al. (2004) suggested. The directional changes towards the lab field in this study is more likely caused by the portion of remanence acquired during the “in-field” step (the so-called “pTRM tails”), which is not fully removed in the subsequent “zero-field” step, as mentioned for the “MD” slag samples in Shaar et al. (2011).
Our IZZI-T results, alternatively, can be analyzed by a bootstrap technique in constraining the API estimate, in a similar way as described in Shaar et al. (2011), because the Arai diagram patterns are likely caused by the influence of partly contained MD particles as mentioned above. The bootstrap technique in this study were performed using a Microsoft Excel sheet and give a 95% confidence interval of API estimates as an overall mean of the specimen-level values, by applying the following procedure:
For the Arai diagram data of each specimen, all API values meeting a loose set of selection criteria (n ≥ 4, f ≥ 0.3, and β ≤ 0.2; see Paterson et al. (2014) for definitions of the statistics) are determined and calculated using the auto interpreter in the Thellier GUI program. The minimum and maximum of the calculated API values for each Arai diagram result are denoted Bmin and Bmax, respectively.
By applying a second screening criteria of Bmax/Bmin ≥ 5, the specimen-level results are selected for the next calculation.
For individual sets of values from the Bmin to Bmax, a re-sampling routine is run, using an Excel sheet, to pick values randomly and generate a large number of combinations (n = 10,000 for this study) of the picked values from individual specimen-level results meeting Bmax/Bmin < 5.
From the 10,000 combinations, a total of 10,000 means are calculated and the 95% confidence interval of their probability distribution is provided as a constraint of mean API estimate we seek.
Results of the bootstrap procedure are summarized in Table 4. Six of the eight specimens exhibit results with Bmax/Bmin ratios of ten or higher, associated with large degrees of the curvature of the Arai diagram result (1.12 to 1.24 in k). Eventually, two specimen-level results (B2C-1-2 and B2C-2-2) that have k values less than 1.00 meet the Bmax/Bmin < 5 criterion and give us a bootstrap-derived 95% confidence interval of 6.6 to 19.7 μT as an estimation of the API at which the Jinchon Basalt was emplaced. It is also recognized that when the bootstrap analysis is run without applying the Bmax/Bmin criteria, the resultant 95% confidence interval is between 9.9 and 24.0 μT, which is biased slightly high compared to that in which Bmax/Bmin < 5 although it is statistically indistinguishable. Given only the current observation, the necessity for the application of the Bmax/Bmin criterion in constraining an API estimate does not seem robust; this is an issue that needs to be checked further with a sufficient number of specimens.
There appears to be no clear relationship between the Bmax/Bmin ratio and the BDS value. The B2C sample, which includes the two B2C-1-2 and B2C-2-2 specimens with Bmax/Bmin < 5, has ~ 0.40 for the average BDS (BDSm in Table 4); the other samples with Bmax/Bmin > 5 have ~ 0.33‒0.47 for the average BDS (see Table 4). We postulate that the relationship might be possibly have been complicated by experimental conditions; for example, the ratio and the angle between the ancient field and the field applied during the Thellier API experiment, which are possible factors of the curvature in Arai diagram for non-SD materials (Biggin 2006; Paterson 2011; Shaar et al. 2011).
Average field intensity during the Early Pliocene
We found that, whether the Bmax/Bmin criterion was applied or not, the IZZI-T-derived confidence interval of average API, 6.6‒19.7 μT or 9.9‒24.0 μT, coincides reasonably with the TS-derived average of 13.1 (± 1.7) μT. This concordance can support the feasibility of using the bootstrap approach in API determination of the Thellier experiments for non-SD-contained materials, as suggested initially by Shaar et al. (2011). We could assign, with high fidelity, the mean field intensity during the Jinchon Basalt emplacement as 13.1 μT; this is a remarkably low value compared to the present-day intensity at the site location (~ 52 µT) and an expected local intensity (~ 28 µT) under the GAD assumption with a VADM of 5 × 1022 Am2.
Our new API data from Baengnyeong Island, despite a geologically short record of the geomagnetic field, provides an opportunity to discuss field behavior during the Early Pliocene, compared with the global API database, such as the PINT (Biggin et al. 2009, 2010). Figure 6a shows previously published data (grey crosses in the figure) of APIs as site/cooling unit-mean estimates for the age interval of 7 to 0.05 Ma, downloaded from the PINT database with version 2015.05 (http://earth.liv.ac.uk/pint/, accessed July, 2018), as a VADM versus age plot, where the VADM values were recalculated from this study using the individual sample latitudes because of mixing of VDM and VADM values and absence of VADM values in some downloaded data. In addition, 24 data points (mean estimates for lava cooling units) reported in Ahn et al. (2016) are newly included in Fig. 6a. We note that these data in the PINT database have highly variable qualities associated with their reliabilities. To view after screening out low-quality data, we apply the quality criteria that each data point has the number used in the PI calculation of three or more (NF ≥ 3), a standard deviation of 20% or less (σF ≤ 20%), and stable polarity of normal or reverse (to omit “transitional” and “unknown” in the dataset), thereby extracting 614 data points fulfilling the quality criteria. Among the extracted data, we further extract only data that were determined by the TS method (LTD-DHT-S) and Thellier (or Thellier-modified) methods with pTRM checks (T+) including the correction technique by Valet et al. (1996) (T + Tv), shown as yellow circles (LTD-DHT-S; n = 79) and blue diamonds (T+ and T + Tv; n = 368) in Fig. 6a.
For the Early Pliocene there are only 23 data points from five studies (Bogue and Paul 1993; Laj et al. 2000; Goguitchaichvili et al. 2001; Tauxe et al. 2004; Yamamoto and Tsunakawa 2005) after the above data selection. The 23 data all were determined by the Thellier-type methods with pTRM checks (T+) or the Tsunakawa–Shaw method (LTD-DHT-S), and most of them are higher than 5 × 1022 Am2 in VADM representing fairly high dipole strengths during the period compared to those of the past few Myr. Our low API estimate from Baengnyeong Island (Korea), using the inclination of our determined in situ ChRM mean and the site latitude, is calculated to be 2.87 (± 0.37) × 1022 Am2 in VDM and 2.32 (± 0.30) × 1022 Am2 in VADM (see also Fig. 6a), respectively. The new VADM data is the second smallest value for the period, inferring a possibility of more large variations in the dipole strength during the period.
Figure 6b shows quartile box plots of the selected VADMs including our new data for four geologic time spans, namely the Early Pliocene (n = 24), Late Pliocene (n = 27), Early Pleistocene (n = 115), and Middle-Late Pleistocene (n = 269), and Fig. 6c shows their associated VADM histograms for the individual periods. For the Middle‒Late Pleistocene the median VADM is as high as ~ 7.5 × 1022 Am2, close to the present-day dipole strength, displaying a distinct bimodal distribution with peaks at the 4‒5 and 7‒8 × 1022 Am2 bins. When going back to the Early Pleistocene and Late Pliocene, VADMs become more concentrated at ~ 5 × 1022 Am2, indicating the median of ~ 5 × 1022 Am2. For the Early Pliocene the median appears to increase slightly (~ 6 × 1022 Am2). However, we also can see that the distributions concentrated around ~ 5 × 1022 Am2 are skewed towards lower values. We emphasize that, currently, it is difficult to say whether the average dipole strength during the Early Pliocene period was moderately high or generally consistent with that over the past ~ 5 Myr (~ 5 × 1022 Am2) and thus further investigation is needed to clarify this issue.
From two sites of basaltic rocks with inferred ages of approximately 4‒5 Ma from Baengnyeong Island, Korea, paleomagnetic and rock magnetic investigations have been performed for the first time. Paleodirectional and absolute paleointensity (API) analyses successfully reconstruct a paleomagnetic record with the VGP position at 70.2° N and 342.1° E and the VDM (VADM) of 2.87 ± 0.37 (2.32 ± 0.30) × 1022 Am2, which is considered as a normal-polarity state within the apparent secular variation range. We could confirm that, even for such samples containing non-SD particles, the Tsunakawa–Shaw (TS) API experiments can successfully give a mean API estimate with high reliability and precision. The IZZI-Thellier experiments with a bootstrap procedure in API determination gave a confirmatory result to support the TS-derived mean estimate; but the Thellier-derived value was not used in the final calculation because of the relatively large uncertainty. Our new API data from Baengnyeong Island give a fairly low dipole strength compared to the global database for the Early Pliocene, thereby indicating larger dispersion in the dipole strength during the period than found in the previous data. Further, it still cannot be certain whether the Early Pliocene dipole strength was moderately high (> 5 × 1022 Am2). To clarify this ambiguity, we encourage further investigations obtaining well-determined API data of the Early Pliocene.
Availability of data and materials
Data are available on request by contacting HSA.
anhysteretic remanent magnetization
bulk domain stability
characteristic remanent magnetization
in-field cooling/zero-field cooling
geocentric axial dipole
isothermal remanent magnetization
- IZZI-T method:
Thellier method with the IZZI protocol (Tauxe and Staudigel 2004) for absolute paleointensity determination
natural remanent magnetization
- TS method:
Tsunakawa–Shaw method for absolute paleointensity determination
virtual (axial) dipole moment
virtual geomagnetic pole
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We thank Dr. Kazuto Kodama and Dr. Youn Soo Lee for designing the sampling campaign, which collected samples analysed in this work, in part of the KIGAM (Republic of Korea)-CMCR (Japan) cooperative research work in 2007. Dr. Y.S. Lee is also appreciated for his help in the field. We thank the editor, Dr. Chuang Xuan, for handling this paper for publication. We are very grateful to Dr. Greig Paterson, Dr. Nobutatsu Mochizuki and one anonymous reviewer for their thorough reviews and helpful comments. This work was supported by a Basic Research Project (GP2017-002‒19-3111-1; Development of Integrated Geological Information Based on Digital Mapping) of the KIGAM, funded by the Ministry of Science and ICT (Information, Communication and Technology). This work was partly supported by JSPS KAKENHI Grant Number 15H05832 and the Basic Science Research Program through the National Research Foundation of Korea (NRF-K) funded by the Ministry of Education (NRF-2016R1D1A1B03935437‒NP2019-004‒19-6823). We would like to thank Editage (http://www.editage.com) for English language editing.
The samples used in this study were collected with the aid of KIGAM and CMCR, Kochi University. The measurements leading to these results were taken under the cooperative research program of CMCR, Kochi University. This study was supported by JSPS KAKENHI Grant Number 15H05832 to YY, and the Basic Research Project (GP2017-002) of the KIGAM funded by the Ministry of Science and ICT and the grant of the National Research Foundation of Korea funded by the Ministry of Education (NRF-2016R1D1A1B03935437) to HSA.
The authors declare that they have no competing interests.
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Ahn, HS., Yamamoto, Y. Paleomagnetic study of basaltic rocks from Baengnyeong Island, Korea: efficiency of the Tsunakawa–Shaw paleointensity determination on non-SD-bearing materials and implication for the early Pliocene geomagnetic field intensity. Earth Planets Space 71, 126 (2019). https://doi.org/10.1186/s40623-019-1107-6
- Baengnyeong island
- Early pliocene
- Non-SD-bearing material
- Tsunakawa–Shaw paleointensity
- Thellier-type paleointensity