The dominant dipolar component of the Earth’s magnetic field has been steadily weakening for at least the last 170 years. Prior to these direct measurements, archaeomagnetic records show short periods of significantly elevated geomagnetic intensity. These striking phenomena are not captured by current field models and their relationship to the recent dipole decay is highly unclear. Here we apply a novel multi-method archaeomagnetic approach to produce a new high-quality record of geomagnetic intensity variations for Hawaii, a crucial locality in the central Pacific. It reveals a short period of high intensity occurring ~1,000 years ago, qualitatively similar to behaviour observed 200 years earlier in Europe and 500 years later in Mesoamerica. We combine these records with one from Japan to produce a coherent picture that includes the dipole decaying steadily over the last millennium. Strong, regional, short-term intensity perturbations are superimposed on this global trend; their asynchronicity necessitates a highly non-dipolar nature.
Evidence that the geomagnetic field has exhibited numerous intense, short-lived, regional maxima in intensity at various times and locations in the last few thousand years is rapidly accumulating: records from Europe1,2, Mesoamerica3,4, West Africa5 and the Middle-East6,7,8 show at least one intensity high. These highly intriguing features are poorly understood because the limited number and uneven geographical distribution of reliable archaeointensity records hamper a meaningful analysis. Current methods to obtain absolute archaeointensities and palaeointensities are only applicable to materials that acquired a thermal remanent magnetization by cooling in the Earth’s magnetic field. Until now, only records using well-dated man-made baked artefacts such as pottery, kilns and copper slags attained the temporal resolution needed to reveal the occurrence of short-lived rapid fluctuations in geomagnetic field intensity. Archaeological artefacts, however, are only available for specific ages and locations linked to ancient civilizations—the majority of data being derived from Europe, the Middle East and Mesoamerica. To provide spatial and temporal constraints on the occurrence of archaeomagnetic intensity highs and to assess the driving mechanism causing these short-lived phenomena, we have to turn to more widely available extrusive rocks. However, as a consequence of their differing composition and thermal history, the success rate in obtaining reliable estimates of the geomagnetic field intensity is much lower for lavas than for archaeological artefacts.
The island of Hawaii (USA) is a particularly important region to obtain a regional curve of geomagnetic field behaviour from because of its location in the central Pacific. Without reliable full vector data from Hawaii, a vast region is not adequately covered in geomagnetic models. Fortunately, numerous well-dated lava flows were emplaced at a relatively high frequency, making it possible to produce curves with high temporal resolution. The palaeointensity of Hawaii is well studied9,10,11,12; however, variations between near-coeval flows are unacceptably large (30–50 μT), testifying to the difficulties associated with obtaining meaningful estimates from lavas.
Here we report the results of archaeointensity experiments performed on samples from well-dated Hawaiian flows using a combination of methodologies. Our multi-method archaeointensity approach and the very strict selection criteria applied to both the data obtained in this study and existing data produce a coherent record of archaeointensity variations for Hawaii for the past ~1,800 years. This record is demonstrated to be robust through the consistency of results produced using very different methods and the agreement with the observational record over the last 170 years. The unusually high temporal resolution in our record is primarily attained by calibrating a non-heating palaeointensity approach—the pseudo-Thellier technique13. We show that this method reconstructs the intensity of the palaeofield reliably from most of the samples that are unsuccessful in conventional archaeointensity methods because of thermally induced alteration. The new Hawaiian archaeointensity record indicates notably high values from ~1000–1150 AD followed by an undulating decrease thereafter. Similar phenomena are observed in Europe 200 years earlier and in Mesoamerica 500 years later. A comparison with these and other records of geomagnetic field variations for the northern hemisphere implies a non-dipole character of such comparatively short-lived intensity highs. Furthermore, they cannot be explained by westward drift of a single geomagnetic phenomenon. We therefore conclude that these rapid regional variations in the intensity of the Earth’s magnetic field result from spatially and temporally non-uniform geomagnetic phenomena that are presently enigmatic in terms of their sources.
We sampled 33 independent cooling units on the Big Island of Hawaii at 43 different locations. At some locations, we sampled multiple sites, often at different depths in the flow. Details of all 63 sampled sites are provided in Supplementary Tables S1, S2. Reliable global estimates of the geomagnetic field intensity are available since 1840 AD14,15; the 37 sites taken from lavas younger than 1840 AD are therefore suitable to verify the archaeointensity methodologies and selection criteria used. The other 26 sites date between 430 and 1840 AD. Localities from before 1790 are radiocarbon-dated, with all dates used in this study originating from two studies16,17; we recalibrated these dates using the latest INTCAL.09-curve18,19.
We applied both thermal20,21 and microwave Thellier-type techniques22 and domain-state-corrected multispecimen archaeointensity experiments23,24 (MSP-DSC). Detailed information on all absolute archaeointensity experiments is provided in the Methods section. Furthermore, we calibrate a non-heating palaeointensity technique, the pseudo-Thellier approach13, to make it suitable to obtain absolute estimates of the intensity of the palaeofield from samples that are unsuccessful in conventional archaeointensity experiments.
In total, 96 samples distributed over all sampled cooling units were subjected to IZZI-Thellier archaeointensity determinations21,25,26. The results were grouped by their age and, if four or more samples passed our selection criteria (see Methods and Supplementary Table S3), their results were averaged. A further criterion was applied requiring that the s.d. of the accepted results was <20% of their mean. Out of 33 cooling units/age groups, just two reliable archaeointensity estimates were obtained and both had post-1840 AD ages (Supplementary Fig. S1, Supplementary Table S4).
Microwave Thellier experiments
The microwave archaeointensity approach emulates the conventional IZZI-Thellier method but uses high frequency microwaves instead of thermal energy to (de)magnetize the samples22,27,28. Microwave archaeointensity experiments were performed using a combination of Thellier-type protocols on 23 samples from four key pre-1840 sites, with just one of these lavas yielding a reliable archaeointensity estimate (see Methods).
Domain-state-corrected multispecimen experiments
Samples from eight of our 63 sites were subjected to MSP-DSC experiments23,24 by virtue of them passing the ‘ARM test’29 for thermally induced alteration. Owing to varying alteration temperatures, MSP-DSC experiments were performed at several different temperatures between 150 and 360 °C. Four of these eight sites were younger than 1840 AD and all these yielded the expected archaeointensity to within 3 μT—that is, accurate to better than 10%. (see Methods, Supplementary Fig. S2, Supplementary Table S5).
Owing to our strict selection criteria, we obtained a reliable estimate of the palaeofield’s intensity for only nine of our 33 possible age groups using conventional archaeointensity methods. A complicating issue with these lavas is that the heating of the samples in conventional archaeointensity experiments frequently induces alteration, rendering the obtained result meaningless. Relative palaeointensity records are frequently obtained from sediments. In relative palaeointensity techniques, the natural remanent magnetization (NRM) of the samples is compared with (progressively increasing) imparted anhysteretic remanent magnetizations (ARMs), thus avoiding heating the samples. The relative pseudo-Thellier technique13 (see Methods) is analogous to the thermal Thellier technique: it compares the demagnetized NRM and the acquired ARM for increasingly higher alternating field (AF) values in an Arai plot (Supplementary Fig. S3). Yu et al.30 explored the potential of using the pseudo-Thellier method on lavas and found that its outcome is dependent on the grain-size distribution of the remanence-carrying grains. To select the pseudo-Thellier results that can be reliably compared, we use a selection criterion based on the grain-size indicator B½ARM, the magnitude of the AF for which half of the maximum ARM is imparted—a parameter that can be obtained directly from the pseudo-Thellier experiments. For the samples younger than 1840 AD, the obtained pseudo-Thellier slopes are divided by the age-equivalent reference values from the GUFM1 (pre-1900) and IGRF (post-1900) models; this ratio is then plotted against the samples’ B½ARM (Fig. 1a). As the pseudo-Thellier slope is linear with the Earth’s magnetic field the samples cooled in, this ratio should yield a constant value for samples with similar pseudo-Thellier behaviour. To assess the feasibility of including samples as a function of B½ARM, the 10-point moving average and its s.d. are determined (Fig. 1a). The s.d. of the moving average of the ratio is a measure of scatter among the samples. It reveals a high degree of scatter for samples with B½ARMs <19.5 mT; and the moving average only becomes constant for samples with a B½ARM >23 mT. We therefore choose 23 mT as the lower limit of the B½ARM window of reliable samples. Fewer data are available to define the upper limit of this window; however, for samples with a B½ARM between 23 and 63 mT, the s.d. of the mean of the ratio is <15% of that mean. Thus, we conclude that samples with a B½ARM between 23 and 63 mT can be safely utilized. For all samples younger than 1840 AD with a B½ARM between 23 and 63 mT, the pseudo-Thellier slopes show a decreasing trend with age (Fig. 1b). We fit the linear trend line through the accepted pseudo-Thellier slopes on the decreasing trend in the GUFM1 and IGRF models (Fig. 1c), yielding a calibration equation to convert pseudo-Thellier slopes into absolute intensity values. This linear relationship is given by: Babs (μT)=7.371 × pseudo-Thellier slope+14.661. It is important to note that this relationship depends on the field strength used to impart the ARM during the pseudo-Thellier experiments (in this study 40 μT, see Methods). The non-zero y axis intercept must be explained by the relationship behaving nonlinearly towards (much) lower intensities (being, for example, a Langevin function). The high degree of agreement between the pseudo-Thellier results and the field models CALS3K.4 (refs 31, 32), CALS10K.1b33, ARCH3K.1 (refs 31, 32), GUFM1 (ref. 14) and IGRF (Fig. 1d) and other archaeointensity methods (Fig. 2) strongly supports that the linear approximation is appropriate for the range used in this study.
For each of our sites, four to ten samples were processed to produce 413 data points in total (Supplementary Table S6); 250 of these are younger than 1840 AD and can be used for calibration purposes. The 413 data points in the pseudo-Thellier data set are grouped by their age; if four or more samples per group pass the selection criterion, the pseudo-Thellier results of those samples are averaged and converted to absolute archaeointensities (Supplementary Table S7). Out of 33 possible age groups, we yield 20 reliable calibrated pseudo-Thellier archaeointensities, a success rate of ~61%; substantially higher than the ~27% success rate associated with our thermal archaeointensity experiments. Furthermore, we resolve the observed trend in the geomagnetic field intensity at Hawaii for the historical age range (Fig. 1d); all the 10 calibrated pseudo-Thellier estimates are within 3 μT of their expected values and randomly distributed about them. This gives confidence that the calibrated pseudo-Thellier palaeointensity approach can reliably be used also for older sites.
Previously reported archaeointensities
Finally, we augmented our measurements with carefully selected data from previous archaeomagnetic studies on Hawaii as provided by the GEOMAGIA database34. We downloaded 107 intensity entries for the age range considered in this paper. First, we only considered intensity entries that have their own 14C dating associated with them; this rejects 42 entries. Second, directional information should be provided along with the intensity data so that virtual dipole moments (VDMs) can be calculated; this information is missing for another 27 entries. Third, we required an entry to be the mean of at least four independent results, with its s.d. being <20% of the mean. As different authors report different Thellier-style parameters, and select their most reliable results accordingly, it was not possible to reinterpret all data and subject them to the same set of selection criteria. Where authors had presented different ‘classes’ of intensity results, only the highest quality subset was taken. We accept 15 archaeointensity entries9,10,11,12,27 from the GEOMAGIA database after our careful selection procedure (Supplementary Fig. S4, Supplementary Table S8). Directional information was accepted if associated 14C ages were provided—a criterion met by 143 entries35 (Supplementary Table S9). Some of the 14C ages associated with either directional or archaeointensity results were not calibrated using a proper radiocarbon calibration curve or were calibrated using a curve that is by now superseded. The original dating-sample codes and 14C laboratory ages were specified in all reporting studies. We therefore recalibrated all specified 14C datings by means of the newest INTCAL.09 curve using the Calib 6.0 routine18,19 (Supplementary Table S9).
We compiled all accepted data into a full vector description of the regional behaviour of the geomagnetic field (Fig. 2). An intensity curve was computed based on maximum likelihoods, together with its one s.d. interval (Fig. 2e,f). The quality of our record is strengthened considerably through the observation that near-coeval archaeointensities obtained using different methods and from different cooling units agree within experimental uncertainty. Different lavas proved to be successful in certain archaeointensity techniques but failed in others; thus, it is important to apply various techniques within one archaeointensity study. Our calibrated pseudo-Thellier method proved to be an important addition to absolute archaeointensity methodologies, elucidating the geomagnetic field intensity for sites that fail in absolute methods. With our new multi-method approach, we were able to obtain reliable archaeointensity estimates for 22 out of the 33 possible ages. This constitutes an unusually high success rate of ~67%, further supporting the application of this approach to future studies aiming to construct a reliable regional full vector record from a volcanic edifice.
The obtained intensity curve shows a constant value of ~40 μT from 200 to ~850 AD. Between ~846 and 977 AD, the field intensity at Hawaii rose quickly from ~40 to ~63 μT. The following short period of very high field intensity up to ~1150 AD is robustly indicated by five results from four lava flows measured using three different techniques. Owing to Hawaii’s low latitude, the high intensity corresponds to a VDM peaking at ~140 ZAm2—75% higher than today’s average value. Between 1120 and 1170 AD, the archaeointensity rapidly decreased again and slowly thereafter, with a modest recovery suggested around 1650 (but note the limited age precision associated with this single result shown in Fig. 2). Although precise estimates of the rates of decrease and increase are hampered by the resolution of our data, average rates of change of at least 150–250 nT per year are associated with the observed intensity high, approximately one order of magnitude higher than today’s rate of decrease at Hawaii.
There are now reliable records of the variation in geomagnetic field intensity for Europe1,2, Mesoamerica3,4, Japan36 and Hawaii for the past 1,600 years; these records are reasonably well distributed over the northern hemisphere (Fig. 3). Apart from the occurrence of short-lived increases in the Hawaiian and Mesoamerican records, the reported virtual axial dipole moments for these four locations are notably similar between 1000 and 2000 AD. This implies a relatively homogenous field behaviour and very likely reflects the dipole decaying steadily from ~105 ZAm2 in 1000 AD to ~85 ZAm2 in 2000 AD—a rate of 2 ZAm2 per century. Immediately before 1000 AD, there was an intensity peak in Western Europe1,2 similar to those observed later in Hawaii and Mesoamerica. The four records show less coherence with one another in this earlier period. It is, however, currently unclear whether this is caused by reduced temporal resolution and therefore reliability in the virtual axial dipole moment curves or increased geomagnetic variability at smaller spatial scales. It is worth noting that this time period is coincident with a relatively reduced dipole component in the global field model CALS10K.1b33.
Overall, it appears that geomagnetic intensity behaviour over the last millennium can be decomposed into two components. The first is a long-term, nearly steady decay in the dipole component extending, backwards, the recent instrumental record-based trend14,15. The second is a series of rapid and severe fluctuations in intensity that our observations exclude as having a significant dipole contribution. They are neither globally synchronous nor exhibit opposite behaviour for locations that differ ~180° in longitude as expected for dipole tilt. It is furthermore unlikely that the observed rapid variations are caused by a single higher-order phenomenon and westward drift, as the peak in Hawaii predates that in Mesoamerica. We therefore conclude that the rapid fluctuations in the last 1,600 years must originate from intense, small-scale and potentially unrelated geomagnetic processes that occur and subside within tens to hundreds of years. Such spatially and temporally non-uniform features are, as yet, entirely enigmatic in terms of their physical cause but appear to be a fundamental trait of the behaviour of the geomagnetic field, and geodynamo operation, on centennial timescales.
Thermal IZZI-Thellier measurements
The thermal Thellier measurements were made on an AGICO JR-5 spinner magnetometer using cubic samples with sides of 10 mm and followed the IZZI-Thellier protocol21,25,26. The temperature steps are as follows (all in °C, Z=zero field, I=in field (35 μT), ZC=tail-check, IC=pTRM-check): 100 Z, 100 I, 150 I, 150 Z, 100 IC, 200 Z, 200 I, 200 ZC, 300 I, 200 IC, 350 Z, 350 I, 350 ZC, 400 I, 400 Z, 350 IC, 450 Z, 450 I, 450 ZC, 480, I, 480 Z, 480 IC, 500, I, 500 Z, 450 IC, 520 I, 520 Z, 480 IC, 530 I, 530 Z, 540 I, 540 Z, 520 IC, 550 I, 550 Z, 560 I, 560 Z, 540 IC, 570 I, 570 Z, 580 I and 580 Z. The program ThellierTool 4.2 (ref. 37) was used for data interpretation. To accept an archaeointensity estimate, at least four samples should pass the SELCRIT-1 selection criteria38,39 (Supplementary Table S3) and the mean should have a s.d. <20% of the mean. Generally, the lower temperature end (below 450 °C) of the Thellier experiments yielded the best results (Supplementary Table S4, Supplementary Fig. S1).
Microwave Thellier measurements
Discs of 5 mm diameter and 2–3 mm thickness were measured using both 14 GHz microwave systems at the University of Liverpool22,27,28. The Coe40,41; IZZI21; and perpendicular42 protocols were applied to test the sensitivity of the results to the methodology. pTRM checks43 and pTRM tail checks44 were applied in some cases. Where the IZZI method or pTRM tail checks were used, the laboratory field was directed at an angle of at least 45° to the NRM so that multidomain effects were not made undetectable through sub-parallelism of the ancient and laboratory field vectors45. A laboratory field of 40 μT was applied in all experiments. As for the IZZI-Thellier experiments, a minimum of four results were required to produce an average required to have a s.d. <20% of the mean. The criteria used for the individual results are specified in Supplementary Table S3.
Domain-state-corrected multispecimen method
For a meaningful MSP-DSC23,24 experiment, a large portion of the NRM, preferably at least 15%, should be unblocked at the temperature used in the experiment (referred to as set temperature); no or very small overprints should be present; and both chemical and magnetic alteration should be avoided. To test for these conditions, at least three samples per site are thermally demagnetized using an ASC-TH48 thermal demagnetizer and measured on a 2G DC-SQUID magnetometer (Supplementary Fig. S2, column a). Furthermore, cyclic low-field susceptibility-versus-temperature analyses were performed on an AGICO KLY-3S susceptometer with furnace attachment (Supplementary Fig. S2, column b). The peak temperatures of the six heating cycles are 220, 290, 360, 420, 500 and 600 °C; after each heating cycle, the temperature is lowered at least 50 °C to test the reversibility of the signal. The highest temperature reached in the last reversible segment is chosen as the ‘alteration temperature’ and is regarded as the highest temperature that can be used safely in thermal archaeointensity experiments.
On the basis of the alteration temperature and the percentage of NRM unblocked, one or more potential set temperatures are chosen per site. For these potential set temperatures, ARM tests29 are performed (Supplementary Fig. S2, column c). For 14 sites in this study that pass the ARM test, the MSP-DSC protocol24 was followed. A test for subtle alteration during the multiple heating steps is incorporated in this protocol; results are only accepted if the alteration during the experiment is ≤3%. Of the 14 MSP-DSC experiments, six passed this last selection criterion. The ‘α-parameter’24 is set to 0.5. To remove potential outliers from the MSP-DSC diagrams, the data points that fall outside the one-s.d. error envelope resulting from all measured data are removed, and the linear fit, together with the corresponding one-s.d. error envelope, is recalculated using only the accepted data points (Supplementary Fig. S2, column d; Supplementary Table S5).
All pseudo-Thellier measurements are performed on a robotized 2G DC-SQUID magnetometer, with demagnetization coils attached to the system; AF fields higher than 100 mT are applied manually in a laboratory-built demagnetization coil. The pseudo-Thellier experiments consist of three steps. First, the NRM of the samples is demagnetized in 18 field steps (0, 2.5, 5, 7.5, 10, 15, 20, 25, 30, 40, 50, 60, 70, 80, 100, 150, 225 and 300 mT). After the demagnetization at 300 mT, the magnetization of the samples is generally reduced to a few per cent of their NRM. The NRM is demagnetized in three perpendicular axes, without aligning the NRM to either one of them. In the second step of the pseudo-Thellier protocol, a sequence of ARMs is imparted on the samples using the same AF field steps as in the NRM demagnetization. The ARM is imparted in the axial direction of the magnetometer system; as anisotropy in extrusive igneous rocks is generally <2%, the NRM and ARM can be reliably compared, even though they may not have the same direction. The DC bias field for the ARM acquisitions is set to 40 μT. The last step of our pseudo-Thellier protocol is to demagnetize the imparted ARMs, again using the same field steps.
To obtain reliable pseudo-Thellier slopes that compare the field in which the NRM was acquired among sites, the same grains that carry the NRM must carry the ARM in the samples. To assess the extent to which this is the case, the demagnetization experiments of the NRM and the ARM (step 1 and step 3) are plotted against each other for each field step (Supplementary Fig. S3, panel a). If the same grains carry the NRM and the ARM, it is to be expected that the demagnetization curves behave proportionally—that is, the fit through the plot of the two is linear. For small AF fields, below 10 mT, small overprints in the NRM or viscous behaviour sometimes causes the data points to deviate from the linear fit. The linear segment is usually between 15 and 100 mT, and these fields are subsequently used to obtain the pseudo-Thellier slope. The AF field segment used is specified per sample in Supplementary Table S6.
The pseudo-Thellier slope is obtained from an Arai plot of the NRM remaining (data from step 1) on the vertical axis against the ARM acquired (step 2) on the horizontal axis (Supplementary Fig. S3, panel b). The pseudo-Thellier slope is (the absolute) slope of the linear fit through the data points corresponding to the AF fields selected above. This slope is a measure of the intensity of the NRM-imparting field with respect to the ARM-imparting field. As the imparting DC bias field is equal for all samples in this experiment, the pseudo-Thellier slope is a relative indicator of the archaeointensity.
How to cite this article: de Groot, L. V. et al. Rapid regional perturbations to the recent global geomagnetic decay revealed by a new Hawaiian record. Nat. Commun. 4:2727 doi: 10.1038/ncomms3727 (2013).
This research was mainly funded by a grant from the Earth and Life Science Division (ALW) of the Netherlands Organization for Scientific Research (NWO). A.J.B. acknowledges NERC Advanced Fellowship NE/F015208/1. This is SOEST contribution 9016 and HIGP-2018. We are grateful for the insightful discussions with the late Tom Mullender; his support and innovative technical solutions are deeply missed.
Supplementary Figures S1-S4 and Supplementary Tables S1-S9
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