Abstract
We present DTU’s candidate field models for IGRF12 and the parent field model from which they were derived, CHAOS5. Ten months of magnetic field observations from ESA’s Swarm mission, together with uptodate ground observatory monthly means, were used to supplement the data sources previously used to construct CHAOS4. The internal field part of CHAOS5, from which our IGRF12 candidate models were extracted, is timedependent up to spherical harmonic degree 20 and involves sixthorder splines with a 0.5 year knot spacing. In CHAOS5, compared with CHAOS4, we update only the lowdegree internal field model (degrees 1 to 24) and the associated external field model. The highdegree internal field (degrees 25 to 90) is taken from the same model CHAOS4h, based on lowaltitude CHAMP data, which was used in CHAOS4.
We find that CHAOS5 is able to consistently fit magnetic field data from six independent low Earth orbit satellites: Ørsted, CHAMP, SACC and the three Swarm satellites (A, B and C). It also adequately describes the secular variation measured at ground observatories. CHAOS5 thus contributes to an initial validation of the quality of the Swarm magnetic data, in particular demonstrating that Huber weighted rms model residuals to Swarm vector field data are lower than those to Ørsted and CHAMP vector data (when either one or two star cameras were operating). CHAOS5 shows three pulses of secular acceleration at the core surface over the past decade; the 2006 and 2009 pulses have previously been documented, but the 2013 pulse has only recently been identified. The spatial signature of the 2013 pulse at the core surface, under the Atlantic sector where it is strongest, is well correlated with the 2006 pulse, but anticorrelated with the 2009 pulse.
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Background
In May 2014, the IAGA task force responsible for IGRF12 requested candidate geomagnetic reference field models [main field (MF) for epochs 2010.0, 2015.0 and predictive secular variation (SV) for 2015.0–2020.0] to be submitted by 1 October 2014. This article describes in detail the candidate models submitted by DTU Space and the timedependent parent model from which they were derived, called CHAOS5.
Geomagnetic field modellers producing candidate models for IGRF12 were in the fortunate position that the European Space Agency (ESA) launched the Swarm satellite constellation, whose aim is to carry out the best ever survey of the Earth’s magnetic field, in November 2013. In parallel with ongoing calibration and validation efforts, ESA promptly released L1b magnetic field data to the scientific community by May 2014. Swarm data were crucial to the DTU candidate models presented below. We therefore describe the selection, processing and modelling of the Swarm data in some detail. In addition to data from Swarm, we used data from previous satellite missions (Ørsted, CHAMP and SACC), along with ground observatory data kindly provided and checked by the British Geological Survey (Macmillan and Olsen 2013).
CHAOS5, the parent model for the IGRF12 candidates reported here, is the latest update of the CHAOS field model series (Olsen et al. 2006; Olsen et al. 2009; 2010; Olsen et al. 2014). The crucial aspects of this model are a timedependent model of the largescale internal field, a static model of the smallerscale internal field, a parameterization of the largescale external field in both solar magnetic (SM) coordinates (with timedependence parameterized by a disturbance index) and geocentric solar magnetospheric (GSM) coordinates, and a coestimation of the Euler angles used for the rotation of the threecomponent vector field from the magnetometer frame to the star camera frame.
The main improvement of CHAOS5 over CHAOS4 is its use of 10 months of Swarm data, as well as more recent ground observatory data. The modelling technique and data selection closely follow those previously described by Olsen et al. (2014). CHAOS5 is similar to the IGRF parent models produced by a number of other teams (for example Maus et al. 2010; Rother et al. 2013; Thomson et al. 2010) in not explicitly modelling the ionospheric field, in contrast to the more sophisticated comprehensive modelling approach (Sabaka et al. 2015; Thébault et al. 2015). Instead, data selection for CHAOS5 is limited to darkregion data from geomagnetically quiet times (when ionospheric currents are weak, at least at nonpolar latitudes), in an effort to isolate as best as possible the field of internal origin.
In the ‘Data’ section, we provide more details concerning the data selection and processing used in the construction of CHAOS5. The ‘Methods’ section gives a brief description of our model parameterization, as well as our chosen procedure for model estimation, including the chosen temporal regularization. Differences between CHAOS5 and CHAOS4 are summarized in Table 1. Details concerning the extraction of the IGRF12 candidate models are given in the section ‘Derivation of candidate models for IGRF12’. In the ‘Results and discussion’ section, results from CHAOS5 are presented, including its fit to ground observatory and satellite data, and the evolution of its model SV, which is, of course, relevant regarding the predictive SV. The time evolution of the secular acceleration (SA) in CHAOS5 is also described, and an interesting new SA pulse at the core surface in 2013 is documented.
Data
Satellite data
Darkregion data from geomagnetically quiet times, suitable for use within the CHAOS field modelling scheme, have been selected. In particular, the following selection criteria, previously used in the CHAOS4 model (Olsen et al. 2014), have again been employed:

Dark regions only (sun at least 10° below the horizon).

Strength of the magnetospheric ring current, estimated using the RC index (Olsen et al. 2014), was required to change by at most 2 nT/h.

Three vector components of the magnetic field were taken for quasidipole (QD) latitudes equatorward of ±55°, while scalar field (intensity) data only were used for higher QD latitudes or when attitude data were not available.

Geomagnetic activity at nonpolar latitudes (equatorward of ±55° QD latitude) was sufficiently low, such that the index Kp≤2^{0}.

Poleward of ±55° QD latitude, scalar data were only selected when the merging electric field at the magnetopause \(E_{m} = 0.33 v^{4/3} B_{t}^{2/3} \sin ^{8/3} \left (\Theta  / 2 \right)\), where v is the solar wind speed, \(B_{t}=\sqrt {{B_{y}^{2}} + {B_{z}^{2}}}\) is the magnitude of the interplanetary magnetic field in the yz plane in GSM coordinates and Θ= arctan(B _{ y }/B _{ z }) (Newell et al. 2007), was sufficiently small. More precisely, the weighted average over the preceding 1 h, E _{ m,12}≤0.8 mV/m.
All satellite data are further weighted proportional to sinθ (where θ is geographic colatitude) to simulate an equalarea distribution. The treatment and processing of Ørsted, CHAMP and SACC data generally follow that previously described for the CHAOS4 field model (Olsen et al. 2014). Figure 1 presents the total number of nonpolar magnetic satellite observations used each month in deriving the low degree part of the CHAOS5 model. Note that because there are three Swarm satellites, and because their data are selected in the same manner, there were a relatively large number of data available since the launch of Swarm in November 2013.
From ESA’s Swarm satellite trio, we used the operational L1b data product MagL, for the 10 months 26 November 2013 to 25 September 2014, release 0302 when available, otherwise release 0301. Data were selected from the three satellites, Swarm A, B and C at 60s intervals unless Flags_B=255 or Flags_q= 255, which specifies nonvalid magnetometer or attitude data (see Olsen et al. 2013, for a more detailed description of the L1b products and related flags). We manually rejected Swarm A data from 29 to 30 January 2014 and 6 February 2014 as well as Swarm C data from 25 to 26 March 2014 and 4, 8 and 11 April 2014 when notably large outliers were identified, likely a result of specific manoeuvres that were carried out on these days. In addition, gross outliers were excluded by requiring that all vector field components be within 500 nT (and the scalar field within 100 nT) of the predictions of a preliminary field model, CHAOS4plus_V4, that we constructed using the satellite and ground observatory data available in August 2014. The Vector Field Magnetometer (VFM) data were also slightly rescaled, pointbypoint isotropically forcing their scalar value to agree with the Absolute Scalar Magnetometer (ASM) data. This was a crude attempt to make the ASM and VFM datasets more consistent, in the absence of a suitable vector field correction at the time of model determination in September 2014. Tests showed that the impact of this scaling on magnetic field models was however small, in part because data from sunlit regions (which have larger ASMVFM differences, see Lesur et al. 2015) were not selected. At polar latitudes, only ASM scalar data were used. In all, we used 3×53,137 (17,485) vector data (scalar data) from Swarm A, 3×53,253 (17,744) from Swarm B and 3×49,984 (16,697) from Swarm C, respectively. The altitude of the three Swarm satellites versus time and the coverage of the selected data as a function of latitude and time are presented in Fig. 2.
Observatory data
Annual differences of revised observatory monthly means (Olsen et al. 2014) for the time interval January 1997 to September 2014 were used as additional observational constraints on the SV. Revised monthly means were derived from the hourly mean values of 159 observatories (locations shown in Fig. 3) which have been carefully checked for trends, spikes and other errors (Macmillan and Olsen 2013). The observatory data were rotated from geodetic to geographic components. Prior to producing monthly means by a robust method based on Huber weights (Huber 1964), we removed estimates of the ionospheric (plus induced) field as predicted by the CM4 model (Sabaka et al. 2004) and the largescale magnetospheric (plus induced) field, as predicted by the preliminary field model CHAOS4plus_V4. After taking annual differences, this resulted in 21,733 values of the first time derivative of the vector field components, d B _{ r }/d t,d B _{ θ }/d t,d B _{ ϕ }/d t with the distribution in time shown in the bottom panel of Fig. 3. We emphasize that CM4based estimates of the ionospheric field were removed only from the hourly mean observatory data during the derivation of revised monthly means (since data from all local times were used) and they were not removed from the darkregion satellite data used.
Methods
Model parameterization
The parametrization of the CHAOS5 field model follows closely that of previous versions in the CHAOS model series (Olsen et al. 2006, 2009, 2010, 2014). We assume measurements take place in a region free from electric currents, in which case the vector magnetic field B may be described by a potential such that B=−∇V. The magnetic scalar potential V=V ^{int}+V ^{ext} consists of V ^{int}, describing internal (core and lithospheric) sources, and V ^{ext}, describing external (mainly magnetospheric) sources and their Earthinduced counterparts. Both internal and external parts are expanded in spherical harmonics. The CHAOS5 model thus consists of spherical harmonic coefficients together with sets of Euler angles needed to rotate the satellite vector field readings from the magnetometer frame to the star camera frame.
Considering first the internal field, we work in an Earthcentred Earthfixed (ECEF) coordinate system using a spherical harmonic expansion
where a=6371.2 km is a reference radius, (r,θ,ϕ) are geographic spherical polar coordinates, \({P_{n}^{m}}\left (\cos \theta \right)\) are the Schmidt seminormalized associated Legendre functions, \(\left \{{g_{n}^{m}},{h_{n}^{m}}\right \} \) are the Gauss coefficients describing internal sources, and N _{int} is the maximum degree and order of the internal expansion. The internal coefficients \(\{{g_{n}^{m}}(t),{h_{n}^{m}}(t)\}\) up to n=20 are timedependent; this dependence is described by order 6 Bsplines (De Boor 2001) with a 6month knot separation and fivefold knots at the endpoints t=1997.0 and t=2015.0. Internal coefficients for degrees 21 and above are static, and a maximum degree of 80 was used during the derivation of the new model for the low degree field (CHAOS5l, where ‘l’ denotes low degrees) described here.
Regarding the external field, we represent the near magnetospheric sources, e.g. magnetospheric ring current, by a spherical harmonic expansion in solar magnetic (SM) coordinates (up to n=2, with a special treatment of the n=1 terms). Regarding remote magnetospheric sources, e.g. magnetotail and magnetopause currents, we use a spherical harmonic expansion in geocentric solar magnetospheric (GSM) coordinates (also up to n=2, but restricted to order m=0):
where θ _{ d } and T _{ d } are dipole colatitude and dipole local time. The degree1 coefficients in SM coordinates are timedependent and are further expanded as
where the terms in brackets describe the contributions from the magnetospheric ring current and its Earthinduced counterpart as estimated by the RC index (Olsen et al. 2014), RC(t)=ε(t)+ι(t). We coestimate the timeindependent regression factors \(\hat {q}_{1}^{0}, \hat {q}_{1}^{1}, \hat {s}_{1}^{1}\) and the timevarying ‘RC baseline corrections’ \(\Delta {q_{1}^{0}}, \Delta {q_{1}^{1}}\) and \(\Delta {s_{1}^{1}}\) in bins of 5 days (for \(\Delta {q_{1}^{0}}\)) and 30 days (for \(\Delta {q_{1}^{1}}, \Delta {s_{1}^{1}}\)), respectively. These allow for differences between the groundbased estimate of the degree 1 external magnetic signal (the RC index) and that inferred from low Earth orbit satellites.
In addition to the above spherical harmonic coefficients, we coestimate the Euler angles describing the rotation between the vector magnetometer frame and the star camera frame. For Ørsted, this yields two sets of Euler angles (one for the period before 24 January 2000 when the onboard software of the star camera was updated and one for the period after that date), while for CHAMP and each Swarm satellite, we solve for Euler angles in bins of 10 days.
The new model described here, derived specifically to produce candidate models for IGRF12, is essentially an update of the model CHAOS4l including 10 months of Swarm data and the latest annual differences of observatory revised month means. We refer to this new parent model as CHAOS5l. It involves timedependent terms (for degrees n=1–20, 18,040 coefficients) and static terms (for n=21–80, 6120 coefficients) together resulting in a total of 24,160 internal Gauss coefficients. The total number of external field parameters is 1301, which is the sum of 5 SM terms (\({q_{2}^{m}}, {s_{2}^{m}}\) for n=2), 3 RC regression coefficients \(\tilde {q}_{1}^{0}, \tilde {q}_{1}^{1}, \tilde {s}_{1}^{1}\), 2 GSM coefficients \(\left (q_{n}^{1, \text {GSM}}, q_{n}^{2, \text {GSM}}\right)\), 949 baseline corrections \(\Delta {q_{1}^{0}}\) and 2×171 baseline corrections \(\Delta {q_{1}^{1}}, \Delta {s_{1}^{1}}\). Considering the Euler angles for the Ørsted, CHAMP and the Swarm satellites yields an additional 3×(2+366+94)=1386 model parameters. This finally results in a total of 24,160+1301+1386=26,847 model parameters to be estimated.
Model estimation and regularization
The model parameters described above for CHAOS5l were estimated from 753,996 scalar data and 3×741,440 vector data by means of a regularized iteratively reweighted leastsquares algorithm using Huber weights, minimizing the cost function
where m is the model vector, the residual vector e=d _{obs}−d _{mod} is the difference between the vector of observations d _{obs} and the vector of model predictions d _{mod}, and \(\underline {\underline {C}}\) is the data error covariance matrix.
In the data error covariance matrix \(\underline {\underline {C}}\), anisotropic errors due to attitude uncertainty (Holme and Bloxham 1996) are considered for the vector field satellite data. A priori data error variances for the scalar field were assumed to be 2.5 nT for Ørsted and 2.2 nT for CHAMP and Swarm, while the attitude uncertainties were allocated as in CHAOS4 (Olsen et al. 2014), but with a pointing uncertainty of 10 arc sec for Swarm vector field data.
\(\underline {\underline {\Lambda }}_{3}\) and \(\underline {\underline {\Lambda }}_{2}\) are block diagonal regularization matrices penalizing the squared values of the third and second, respectively, time derivatives of the radial field B _{ r } at the core surface. \(\underline {\underline {\Lambda }}_{3}\) involves integration over the full timespan of the model, while \(\underline {\underline {\Lambda }}_{2}\) involves evaluating the second time derivative only at the model endpoints t=1997.0 and 2015.0. The parameters λ _{3} and λ _{2} control the strength of the regularization applied to the model time dependence during the entire modelled interval and at the endpoints, respectively. We tested several values for these parameters and finally selected λ _{3}=0.33 (nT/year ^{3})^{−2} (the same as used in CHAOS4l) and λ _{2}=100 (nT/year ^{2})^{−2} (a stronger endpoint constraint than used in CHAOS4l). In addition, all zonal terms were treated separately (in CHAOS4l, only the axial dipole was treated separately), with λ _{3} increased to 100 (nT/year ^{3})^{−2}, since we found these internal field components were more strongly perturbed by (i) unmodelled external field fluctuations and (ii) shortcomings in the data coverage due to lack of data in the summer polar region. The regularization parameters were chosen following a series of experiments, primarily relying on comparisons to the SV recorded at ground observatories.
Since both scalar data and Huber weights are involved, the cost function depends nonlinearly on the model parameters. The solution to the minimization problem was therefore obtained iteratively using a Newtontype algorithm. The starting model was a single epoch model with linear SV centred on 2010.0. The final model was obtained after six iterations, by which point sufficient convergence was obtained with the rms misfit converging to better than 0.01 nT and the Euclidean norm of the model change in the final iteration less than 0.005 % that of the model itself.
The complete CHAOS5 field model was obtained in a final step by combining the spherical harmonic coefficients of new model CHAOS5l with the previous CHAOS4h model (Olsen et al. 2014), which in September 2014 was our best model for the highdegree lithospheric field. The transition between these models was implemented at n=24 as for CHAOS4. The various differences between CHAOS5 and CHAOS4 are collected for reference in Table 1. Note that the model statistics reported below are those for CHAOS5l, the parent model from which our IGRF12 candidate models were extracted.
Derivation of candidate models for IGRF12
IGRF12 candidates were extracted from the parent model CHAOS5l as follows:

DGRF, epoch 2010.0
The parent model CHAOS5l, with its splinebased time dependence, was evaluated at epoch 2010.0, and the internal spherical harmonic coefficients up to degree and order 13 output to 0.01 nT.

IGRF, epoch 2015.0
The parent model CHAOS5l, with its splinebased time dependence was evaluated at epoch 2014.75, the end of the month when the last input satellite data were available to constrain the model. The resulting coefficients were then propagated forward to epoch 2015.0, using the linear SV evaluated from CHAOS5l in epoch 2014.0 (as in our SV candidate, to avoid spline model endeffects) as follows:
$$ {}{g^{m}_{n}}(t=2015.0)={g^{m}_{n}}(t=2014.75) + 0.25\cdot \dot{g}^{m}_{n}(t=2014.0) $$((5))Here \({g^{m}_{n}}\) represents each of the Gauss coefficients \(\{{g_{n}^{m}},{h_{n}^{m}}\}\), while \(\dot {g}^{m}_{n}\) represents the SV coefficients \(\{\dot {g}_{n}^{m},\dot {h}_{n}^{m}\}\) in nT/year. The resulting internal spherical harmonic coefficients for the internal field in epoch 2015.0 up to degree and order 13 were output to 0.01 nT.

Predicted average SV, 2015.0 to 2020.0
Since there can be spline model endeffects in the secular acceleration (SA), we evaluated the SV from CHAOS5l at epoch 2014.0, rather than in 2015.0, and did not attempt any extrapolation. These endeffects are essentially due to the lack of ‘future’ data for constraining the SV and SA at the model endpoint, and because SV estimates based on annual differences of ground observatory monthly means are available only up to 6 months before the latest available ground observatory data. It should also be noted that the SV in a splinebased model such CHAOS5l at a particular epoch is not the true instantaneous SV, but a weighted time average, with the amount of time averaging varying with spherical harmonic degree according to the imposed regularization.
The SV spherical harmonic coefficients (first time derivative of the spline model) for the internal field in epoch 2014.0, up to degree and order 8, were then output to 0.01 nT/year. We also provided SV predictions to degree and order 13 as a test secular variation model.
No uncertainty estimates were provided with our candidate models, since we are unable to calculate satisfactory estimates. The largest errors are likely biases caused by unmodelled sources (Sabaka et al. 2015) which cannot be assessed using a formal model error covariance matrix, or by constructing models using the same technique from independent datasets.
Results and discussion
Fit to satellite data
Statistics for the misfit between the CHAOS5l parent field model and the observations used to derive it are collected in Table 2, using the (B _{ B },B _{⊥},B _{3}) notation of Olsen (2002) that is relevant when describing anisotropic pointing errors. The weighted rms misfits to the Ørsted, CHAMP and SACC data are similar to those found previously for CHAOS4l. Regarding the Swarm data, the Huber weighted rms misfits to scalar intensity data (F _{nonpolar}+B _{ B }) of 2.09 nT for Swarm A, 2.07 nT for Swarm B and 2.09 nT for Swarm C are very similar to that found for the CHAMP data, 2.07 nT, considering all 10 years of operation. However, the misfit to the other two vector field components (B _{⊥} and B _{3}) was approximately 0.5 nT lower for Swarm data compared to CHAMP data (note the distinction between B _{⊥} and B _{3} is arbitrary for Swarm, while CHAMP data with either one or two star cameras operating have been considered). This difference mapped into lower misfits to Swarm data in the B _{ r } and B _{ θ } geographic components (e.g. the Huber weighted rms misfit for B _{ r } was 2.77 nT for CHAMP compared to 1.83 nT, 1.99 nT and 1.93 nT for Swarm A, B and C, respectively).
The residuals between CHAOS5l and the Swarm magnetic field data show the expected trends as function of geomagnetic latitude (see Fig. 4, left panel), with the scalar residuals being much larger in the polar region and minimum close to ±35° geomagnetic latitude, where the perturbations due to unmodelled ring current fluctuations are perpendicular to the dipoledominated main field. The Huber weighted residuals as a function of time for Swarm A, B and C at this geomagnetic latitude (±35°) are presented in Fig. 4, right panel. Residuals are usually less than ±5 nT for all three satellites at this location, with similar trends seen for each satellite.
Fit to observatory monthly means
The fit of CHAOS5l to annual differences of observatory monthly means is similar to that obtained for the previous CHAOS4l model, with the rms Huber weighted misfits for d B _{ r }/d t, d B _{ θ }/d t and d B _{ ϕ }/d t of 3.91, 3.83 and 3.12 nT/year, respectively. Examples of comparisons between the SV predicted by CHAOS5l and SV estimates from annual differences of monthly means at selected observatories are presented in Fig. 5. CHAOS5l succeeds in reproducing the SV trends on timescales of 2 years and longer at these observatories. The SV obtained from CHAOS5l thus appears reasonable, at least up to the time of the latest available observatory SV estimates, from early 2014 (using annual differences of monthly means up to August 2014). There is a clear improvement in the SV predicted by the CHAOS5 compared to that predicted by CHAOS4 in 2013 and 2014 (e.g. d B _{ r }/d t at HER, d B _{ θ }/d t at NGK, KAK, d B _{ ϕ }/d t at HON, HER).
Time dependence of secular variation coefficients
The time evolution of the SV in CHAOS5l for degrees 1 to 8 is presented in Fig. 6, 7 and 8, with the SV from CHAOS4l again shown for reference. The two models agree well until approximately 2013, after which the SV from CHAOS4l diverges from that of CHAOS5l, particularly in the lowest degrees which were least regularized. Note that penalization of SA at the model endpoints was imposed more strongly in CHAOS5l; hence, its SV is close to constant near the ends of the model timespan. In addition, the zonal terms (m=0), which sometimes showed spurious SV trends close to the endpoints in CHAOS4 (e.g. in \(d{g^{0}_{1}}/dt\), \(d{g^{0}_{2}}/dt\)) were damped more heavily in CHAOS5l.
Spectral properties of DTU IGRF12 candidate models
The power spectra of the DTU candidate MF and SV models for IGRF12 are presented in Fig. 9, along with spectra of comparable models from IGRF11, the MF in 2010.0, and the predicted SV for 2015.0 to 2020.0. The spectra of our IGRF12 MF candidates are very similar to those of the IGRF11 MF in 2010.0. The spectrum of the difference between our DGRF2010 candidate and IGRF2015 candidate, divided by 5 to get a change per year, is also very close to the spectrum of the predicted SV for 2010.0 to 2015.0 from IGRF11 (Finlay et al. 2010). In comparison, the spectrum of our new SV candidate for 2015.0 to 2020.0 contains slightly more power at degrees 3 to 5, but is otherwise similar.
Rationale for choice of SV candidate
The construction and evaluation of SV candidates have long been considered the most challenging aspects of producing a new IGRF generation (Lowes 2000). Here, we derived our IGRF12 SV candidate taking the position that it is not yet possible to reliably predict future SA events (for example related to geomagnetic jerks) since prognostic forward models capturing the relevant core physics on short time scales are not yet available. We therefore take our estimate of the current SV to be our prediction of the SV for 2015.0 to 2020.0, essentially assuming no average SA or equivalently that the SA will average to zero over the upcoming 5 years. As discussed above, we take the SV from 2014.0 in our spline model as our estimate of the present SV, to avoid problems related to spline model endeffects.
Secular acceleration pulses in 2006, 2009 and 2013
Pulses of SA at the core surface have been identified in the past decade (Chulliat et al. 2010), primarily using data collected by the CHAMP satellite. They are thought to underlie localized rapid secular variation events observed at the Earth’s surface (Lesur et al. 2008; Olsen and Mandea 2008) and the wellknown geomagnetic jerks seen in ground observatory data (Chulliat et al. 2010). Previous studies have highlighted two pulses in 2006 and 2009 in opposite directions (Chulliat and Maus 2014; Olsen et al. 2014). These SA pulses are clearly evident when plotting the time evolution of the SA power integrated over the core surface, as given by
for example, as shown in Fig 10. Here, we take c= 3480 km to be the radius of the core surface, \(\left \{\ddot {g}^{m}_{n}, \ddot {h}^{m}_{n} \right \}\) are the Gauss coefficients for the SA, evaluated from the sixthorder spline model, and we have chosen the degree of truncation N _{SA}=8, to reflect those degrees in which we see wellresolved time dependence of the SV. In Fig 10, we plot S _{ A }(t) from both CHAOS4 and the new CHAOS5 model. They agree rather well up until 2011, although we find slightly more SA power in the 2009 pulse in CHAOS5. The major difference between CHAOS4 and CHAOS5 is a strong SA pulse seen in 2013 in CHAOS5. There was possibly already weak evidence for a pulse around 2013 in CHAOS4, but the sparsity of satellite data in this model after 2010, and the closeness of the pulse to the model endpoint, made interpretation of this feature difficult. Evidence for the 2013 pulse was first presented at the third Swarm Science Meeting (Copenhagen, June 2014) by two independent teams. Chulliat, Alken and Maus (see Chulliat et al. 2015) highlighted evidence derived from DMSP satellite data, while the present authors showed results from a preliminary version of CHAOS5.
Chulliat and Maus (2014) pointed out that the dominant signatures of the 2006 and 2009 pulses in the radial SA at the coremantle boundary, found in the lowlatitude Atlantic sector, are essentially anticorrelated. In CHAOS5, we find that for the new pulse in 2013, the radial SA signature in the Atlantic sector is again correlated with the 2006 pulse and anticorrelated with the 2009 pulse, as shown in Fig. 11. A detailed discussion of this point, and corroborating evidence obtained from the DMSP satellites, is given by Chulliat et al. (2015).
A striking example of the oscillatory core surface SV that now requires an explanation is that the strongest feature in the radial SA under the eastern edge of Brazil was negative in 2006, positive in 2009 and negative again in 2013. Gillet et al. (2015) have proposed that such events can be explained by oscillations in the nonzonal (i.e. nonaxisymmetric) part of the azimuthal (eastwest) quasigeostrophic core flow at low latitudes. Chulliat et al. (2015) suggest an alternative idea that fast equatorial MHD waves in a stratified layer at the top of the core may be responsible. The identification of the 2013 pulse in CHAOS5 opens the door to further detailed study of such hypotheses. The occurrence of SA pulses in 2006.2, 2009.2 and 2013.9 also leads us to wonder whether the next pulse, expected to have the same polarity as the 2009 event, might occur around 2016, before the end of the nominal Swarm mission. Since Swarm should be providing highquality magnetic field measurements with unprecedented spacetime coverage throughout this period, it promises to be an exciting opportunity to characterize a SA pulse in great detail.
Conclusions
We have presented the CHAOS5 geomagnetic field model, including the parent model CHAOS5l from which DTU’s candidate field models for IGRF12 were derived. Details of the magnetic data used to construct CHAOS5 (including their selection and processing) have been documented, with a focus on data from ESA’s Swarm satellite constellation. The CHAOS5 model parameterization and estimation scheme has been reported, and details given concerning how the candidate field models for IGRF12 were extracted.
We find acceptable misfits of CHAOS5 to both ground observatory and Swarm data in 2014, and no evidence of unreasonable model oscillations or spurious trends. CHAOS5 thus provides a consistent representation of magnetic data from six independent satellites (Ørsted, CHAMP, SACC and Swarm A, B, C), as well as ground observatory data, between 1999 and 2015. The Huber weighted rms misfit of the CHAOS5 model to the Swarm vector field data is found to be lower than the Huber weighted rms misfit to the Ørsted and CHAMP vector field data (where either 1 or 2 star cameras were operating), for example considering the radial field component, Huber weighted rms misfits of 1.83, 1.99 and 1.93 nT to Swarm A, B, C data were obtained, compared to 2.77 nT for CHAMP. Overall, the Swarm data seems very well suited for geomagnetic field modelling, and we had no hesitation in using field models based on Swarm L1b magnetic field data, version 0301/0302, to construct our IGRF12 candidate models.
CHAOS5 provides evidence of a secular acceleration pulse around 2013 at the core surface. The amplitude of this new 2013 pulse appears to be larger than the 2009 pulse, and in the Atlantic sector of the core surface, its spatial pattern is well correlated to the 2006 pulse and anticorrelated to 2009 pulse (see also Chulliat et al. 2015). If another pulse happens around 2016, then Swarm will be ideally placed to provide a much more detailed characterization of this presently poorly understood phenomenon.
The CHAOS5 model, as well as the Matlab software to evaluate it, is available from www.spacecenter.dk/files/magneticmodels/CHAOS5/.
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Acknowledgements
We wish to thank Benoit Langlais, an anonymous reviewer, and the guest editor Erwan Thébault for constructive comments that helped us to improve the manuscript. ESA is thanked for providing prompt access to the Swarm L1b data. The staff of the geomagnetic observatories and INTERMAGNET are thanked for supplying highquality observatory data, and BGS is thanked for providing us with checked and corrected observatory hourly mean values. The support of the CHAMP mission by the German Aerospace Center (DLR) and the Federal Ministry of Education and Research is gratefully acknowledged. The Ørsted Project was made possible by extensive support from the Danish Government, NASA, ESA, CNES, DARA and the Thomas B. Thriges Foundation. Support for CCF by the Research Council of Norway through the Petromaks programme, by ConocoPhillips and Lundin Norway, and by the Technical University of Denmark is highly appreciated.
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CCF derived the CHAOS5 field model, extracted the IGRF12 candidate models, and drafted the manuscript. NO developed the CHAOS field modelling software and participated in the design of the study. LTC carried out preparation and preprocessing of Oersted and Swarm data. All authors read and approved the final manuscript.
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Finlay, C.C., Olsen, N. & TøffnerClausen, L. DTU candidate field models for IGRF12 and the CHAOS5 geomagnetic field model. Earth Planet Sp 67, 114 (2015). https://doi.org/10.1186/s4062301502743
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DOI: https://doi.org/10.1186/s4062301502743