Non-monotonic growth and motion of the South Atlantic Anomaly

Abstract

The South Atlantic Anomaly (SAA) is a region at Earth’s surface where the intensity of the magnetic field is particularly low. Accurate characterization of the SAA is important for both fundamental understanding of core dynamics and the geodynamo as well as societal issues such as the erosion of instruments at surface observatories and onboard spacecrafts. Here, we propose new measures to better characterize the SAA area and center, accounting for surface intensity changes outside the SAA region and shape anisotropy. Applying our characterization to a geomagnetic field model covering the historical era, we find that the SAA area and center are more time dependent, including episodes of steady area, eastward drift and rapid southward drift. We interpret these special events in terms of the secular variation of relevant large-scale geomagnetic flux patches on the core–mantle boundary. Our characterization may be used as a constraint on Earth-like numerical dynamo models.

Introduction

The South Atlantic Anomaly (SAA) is a region at Earth’s surface where the intensity of the magnetic field is particularly low. This leads to penetration of solar energetic particles deep into Earth’s atmosphere, posing severe problems for airplanes and ships positioning systems as well as spacecraft electronic systems (Konradi et al. 1994; Deme et al. 1999; Heirtzler 2002; Lean 2005; Auvergne et al. 2009; Domingos et al. 2017). Understanding the past and present locations and mobility as well as the future trajectory of the SAA is both a fundamental scientific challenge—it involves understanding the working of the geodynamo and the impact of core–mantle coupling on core dynamics, as well as an important societal issue—it has major consequences for the operation and protection of surface instruments and spacecrafts, from global positioning systems to the Hubble Space Telescope, which cannot obtain observations over the SAA region.

The current location of the SAA center in Brazil is related to the location of reversed geomagnetic flux patches (RFPs) at the core–mantle boundary (CMB) (Bloxham et al. 1989; Olson and Amit 2006) though this relation is not trivial (Terra-Nova et al. 2017). It is under debate whether the current SAA location represents a persistent boundary-driven feature of Earth’s magnetic field or it is chaotically variable. Based on a data assimilation scheme, Aubert (2015) predicted that the SAA will drift in the near future to the Pacific, i.e. it may suggest a transient feature of the geodynamo. However, the centennial forecast of Aubert (2015) is too short to determine with confidence the long-term behavior of the SAA. In contrast, based on archeological materials, it was argued that the SAA has influenced the surface geomagnetic field for several millennia in Africa (Tarduno et al. 2015; Hare et al. 2018) and South America (Trindade et al. 2018; Hartmann et al. 2019). Tarduno et al. (2015) used such local intensity and directional timeseries, together with observation of a Large Low Shear Velocity Province (LLSVP) in the lowermost mantle below Africa coincident with a historical African RFP on the CMB (e.g. Jackson et al. 2000), to propose that core flux expulsion occurred preferentially at the edge of the LLSVP. In this model, RFPs form stochastically at the LLSVP edge and are then advected westward. A prediction of this model was that a low intensity feature observed in the African archeomagnetic record would be observed later in South America (Tarduno 2018). This scenario is in agreement with subsequent archeomagnetic intensity timeseries from South America and is supported by some synthetic kinematic scenarios (Trindade et al. 2018). The time lag between the Africa and South America surface minima, however, requires frequent expulsion of multiple RFPs (Trindade et al. 2018).

Because of the limited amounts of archeomagnetic data from the southern hemisphere, care must be taken in the interpretation of any archeomagnetic field models applied to the SAA region. Nevertheless, some interesting results have been reported that may guide further data collection. For example, some archeomagnetic field models exhibit persistent surface intensity minimum in the South Atlantic (Brown et al. 2018; Hellio and Gillet 2018; Panovska et al. 2019). Campuzano et al. (2019) found evidence that the SAA has been expanding and westward drifting since 1400.

Heterogeneous CMB conditions may affect the morphologies of outer core convection and the induced geomagnetic field. Numerical dynamo simulations with imposed tomographic outer boundary heat flux have been widely applied to explore geodynamo features, most commonly preferred locations of intense geomagnetic flux patches on the CMB (Gubbins et al. 2007; Aubert et al. 2008; Amit et al. 2015). Terra-Nova et al. (2019) applied such models to show that the longitude of the SAA center may be mantle controlled; However, recovering its relatively large latitude remains a challenge.

Geomagnetic field models spanning the historical era (e.g. Jackson et al. 2000) and more recent modern periods (e.g. Finlay et al. 2010) may provide reliably the location, mobility and area of the SAA. However, previous SAA characterizations which are useful in the context of space safety, can be improved and designed to be more useful for exploring its core dynamical origin. In this paper, we will show that SAA area estimates based on a fixed threshold (De Santis et al. 2013; Pavón-Carrasco and De Santis 2016; Campuzano et al. 2019) are affected by global variations and as such might not represent adequately regional morphological changes of the geomagnetic field. Furthermore, SAA center estimates based on surface minimum positions (e.g. Terra-Nova et al. 2017) do not take into account anisotropic SAA shape. In order to better understand the kinematic origin of the SAA and constrain numerical dynamos (Terra-Nova et al. 2019), a more appropriate characterization of the SAA in terms of its area and center is required.

Previous studies characterized the SAA at altitudes of $\sim 800$ km above Earth’s surface, corresponding to low-Earth orbits of satellites (Casadio and Arino 2011; Schaefer et al. 2016; Anderson et al. 2018). Here, we characterize the SAA at Earth’s surface where geomagnetic observations have been continuously acquired since the advent of intensity measurement (Jackson et al. 2000). We then explore the outer core kinematic origin of the SAA temporal variability.

The paper is outlined as follows. In Sect. "Method" we introduce and justify our new measures of the SAA area and center. The results for this SAA characterization are presented in Sect. "Secular variation of the area and center of the South Atlantic Anomaly" and the kinematic interpretations in terms of temporal evolution of relevant flux patches on the CMB are given in Sect. "Outer core kinematic interpretation". We conclude our main findings in Sect. "Conclusions".

Method

We compare the characterization of the SAA based on previous studies vs. our proposed measures. This characterization includes both the area and the coordinates of the SAA center.

Previous studies defined the SAA area as that where the geomagnetic field intensity $|{\vec {B}}|$ at Earth’s surface is lower than 32,000 nT (De Santis et al. 2013; Pavón-Carrasco and De Santis 2016):

$$\begin{aligned} |{\vec {B}}|<32,000\, \mathrm{nT}. \end{aligned}$$

(1)

From hereafter we term the area based on (1) as S0. This definition is practical for space safety purposes. However, from a more fundamental point of view, (1) is affected not only by regional spatio-temporal field variations, but also by global changes. Fig. 1 illustrates this point. Under a hypothetical scenario of entire field magnitude decrease with no pattern change, a fixed critical threshold (such as 32,000 nT) for the SAA would suggest that its area increases despite no regional variation.

Fig. 1

Schematic illustration of a cross section of the surface field intensity under a global decrease in field intensity from time t1 to time t2. In this scenario, the apparent SAA area based on S0 (1) increases

To overcome this possible problem, alternatively, we factor the critical intensity value by the instantaneous mean surface intensity outside the SAA normalized by its value at the middle of the investigated period, which we term $F_{\mathrm{out}}$:

$$\begin{aligned} F_{\mathrm{out}}={{\int _0^{2\pi } \int _0^{\pi /2} |{\vec {B}}|(t) \sin \theta d\theta d\phi + \int _{\pi/2}^{3\pi /2} \int _{\pi /2}^\pi |{\vec {B}}|(t) \sin \theta d\theta d\phi } \over {\int _0^{2\pi } \int _0^{\pi /2} |{\vec {B}}|(1930) \sin \theta d\theta d\phi + \int _{\pi /2}^{3\pi /2} \int _{\pi /2}^\pi |{\vec {B}}|(1930) \sin \theta d\theta d\phi } }. \end{aligned}$$

(2)

For this purpose, for the area outside the SAA, we consider the northern hemisphere plus the Pacific (i.e. between $90^\circ \hbox {E}$ and $270^\circ \hbox {E}$) southern hemisphere:

$$\begin{aligned} |{\vec {B}}|<32000 F_{\mathrm{out}} \, {\mathrm{nT}}, \end{aligned}$$

(3)

where $\phi$ and $\theta$ are longitude and co-latitude, respectively. Similar planetary-scale averages were recently invoked to quantify the Pacific/Atlantic geomagnetic SV dichotomy (Dumberry and More 2020) or the northern/southern differences in the SV-induced neutral density of the thermosphere (Cnossen and Maute 2020). Note that while the choice of the mid-term year 1930 in the denominator of (3) is completely arbitrary, this has no consequence on the resulting rate of change of the SAA area. From hereafter, we term the area based on (3) as S1. With this definition, the critical value varies with the mean surface intensity away from the SAA. As such, it captures the regional variation of the SAA area, independent of the change in the field magnitude elsewhere.

Next, previous studies tracked the SAA center based on the point of minimum field intensity, both at Earth’s surface (Hartmann and Pacca 2009; Finlay et al. 2010; Aubert 2015; Terra-Nova et al. 2017, 2019) and at higher altitudes (Anderson et al. 2018). Following Terra-Nova et al. (2017), we reproduce this result by first searching for the grid point with lowest intensity and then applying second-order polynomial interpolations using two neighboring points in each direction to resolve off-grid values. From hereafter, we term these coordinates as Min. Note that this definition of a center is advantageous in some useful applications, e.g. in determining the maximum cutoff of radiation vs. duration at a certain radiation level for a spacecraft traversing the SAA. In the context of a core origin, if the shape of the SAA is significantly anisotropic, the minimum point might not well represent the center of the structure (for an illustration see Fig. 2).

Alternatively, centers of mass were invoked to identify and track centers of intense flux patches on the CMB in numerical dynamos (Amit et al. 2010) and geomagnetic field models (Amit et al. 2011). Centers of mass were also used to identify the SAA at $\sim 800$ km altitude (Casadio and Arino 2011; Schaefer et al. 2016). Here, we calculate centers of mass to determine the longitude and co-latitude of the SAA center, $\phi _{\mathrm{cm}}$ and $\theta _{\mathrm{cm}}$, respectively, at Earth’s surface:

$$\begin{aligned} \phi _{\mathrm{cm}}= & {} {{\sum _S \phi _i w_i}\over {\sum _S w_i}}, \end{aligned}$$

(4)

$$\begin{aligned} \theta _{\mathrm{cm}}= & {} {{\sum _S \theta _i w_i}\over {\sum _S w_i}}. \end{aligned}$$

(5)

The summations in (4)–(5) are over the SAA area, either S0 or S1, which we term CM0 and CM1, respectively. The weight w is given by the inverse of the intensity

$$\begin{aligned} w_i={{1}\over {|{\vec {B}}_i|}}. \end{aligned}$$

(6)

Determining the center of the SAA based on the center of mass of its area well represents the center even if its shape is significantly anisotropic.

Fig. 2

Schematic illustration of a cross section of the surface field intensity with an anisotropic configuration. The SAA center based on the minimum (Min, denoted by a point) does not represent well the center of the anomaly. The center of mass method (CM0 or CM1) gives an adequate center denoted by a diamond

Finally, we monitor the time dependence of the value of minimum surface intensity $|{\vec {B}}|_{\rm min}$. In addition, we define a relative minimum surface intensity $|{\vec {B}}|_{\mathrm{min}}^{\mathrm{rel}}$ with respect to the instantaneous field intensity outside the SAA. Similar to (3), we calculate $|{\vec {B}}|_{\mathrm{min}}^{\mathrm{rel}}$ using $F_{\mathrm{out}}$ (2) as follows:

$$\begin{aligned} |{\vec {B}}|_{\mathrm{min}}^{\mathrm{rel}}=|{\vec {B}}|_{\mathrm{min}}/F_{\mathrm{out}}. \end{aligned}$$

(7)

Both areas S0 and S1 were calculated using a simple trapezoid numerical scheme. Tests of the dependence of the results on the grid size show very weak sensitivity and fast convergence with increasing resolution. For all calculations we used a $1^\circ \times 1^\circ$ grid in longitude and co-latitude. With this grid size, the computed properties (i.e. the area and coordinates of the center) practically reach asymptotic values with decreasing grid size.

Secular variation of the area and center of the South Atlantic Anomaly

We used the COV-OBS.x1 time-dependent geomagnetic field model (Gillet et al. 2015) for the period 1840–2020. This model is advantageous for two main reasons. First, it covers the entire historical period, allowing to avoid different field models constructed based on different methods for different epochs (as was previously done in the SAA context by, e.g. Pavón-Carrasco and De Santis 2016; Terra-Nova et al. 2017). Second, COV-OBS.x1 is an ensemble of 100 realizations generated by a stochastic process from estimated mean and covariance of the model coefficients. This approach accounts for the lower precision of geomagnetic data at earlier times and for the uneven geographical distribution of geomagnetic data (Gillet et al. 2013). The 100 realizations represent 100 possible combinations of Gauss coefficients with comparable misfit to the observations.

Figure 3 shows the intensity of the geomagnetic field at Earth’s surface for four snapshots. Before 1930 (Fig. 3, top), the SAA area based on S0 (green dashed contour) was smaller than the area based on S1 (purple dashed contour); whereas after 1930 (Fig. 3, bottom), the area based on S0 was larger. This is trivially expected from the definition of S1 (3). However, the visible differences between S0 and S1 in Fig. 3 provide testimony to the contribution of the temporal variability of the surface intensity outside the SAA to the apparent increase of the SAA area. The centers of the SAA based on Min, CM0 and CM1 are very similar at early snapshots when the SAA area was rather isotropic. However, towards present day the shape of the SAA became more complex with thin branches extending to equatorial east Pacific and South Africa. This anisotropic shape produced significantly different centers for Min, CM0 and CM1.

Fig. 3

Geomagnetic field intensity at Earth’s surface for the mean model of COV-OBS.x1 at four snapshots (Gillet et al. 2015). Dashed green contours denote the S0 area, dashed purple contours denote the S1 area. Green diamonds denote the Min center, green and purple circles denote the centers of mass CM0 and CM1, respectively. Note the different scales from top to bottom

Figure 4 quantifies the characterization of the SAA over the entire period 1840–2020. Overall, the minimum intensity (purple in Fig. 4a) has been monotonically decreasing, except for the period $\sim 1890$–1920 when it deviated from the overall linear trend. The relative minimum intensity (7) even shows a mild increase in that period (turquoise in Fig. 4a). The increase of the SAA area (Fig. 4b) based on S0 (yellow) is quite monotonic. Less so is the evolution of S1 (turquoise), including a period between $\sim 1890$ and 1940 (see dashed vertical lines in Fig. 4) when S1 was flat. The longitude of the SAA center (Fig. 4c) based on Min (purple) has been monotonically decreasing, corresponding to a westward drift. In contrast, the SAA center longitudes based on CM0 (yellow) and CM1 (turquoise) are more variable. Most of the time, the SAA based on these two models have also been drifting westward, but significantly slower. Moreover, between $\sim 1940$ and 1980, CM0 and CM1 have been drifting eastward. The latitude of the SAA center (Fig. 4d) has been decreasing, corresponding to a southward drift. According to Min (purple), this southward drift has been decaying with time. The CM0 (yellow) and CM1 (turquoise) latitudes were fairly flat before $\sim 1900$ and after $\sim 1980$; whereas in between these two epochs, both models exhibited a rapid southward drift. Overall, the SAA area and motion based on the previously proposed models S0 and Min are rather monotonic; whereas in our preferred models S1 and CM1, the SAA area and motion are more non-linear including special events with distinctive trends.

Fig. 4

SAA characterization vs. time for the period 1840–2020. Dark lines denote the mean model of COV-OBS.x1, light envelopes denote the 100 realizations of the ensemble. a Minimum intensity (purple) and the relative minimum intensity $|{\vec{B}}|_{\mathrm{min}}^{\mathrm{rel}}$ (turquoise). b Area based on S0 (yellow) and S1 (turquoise). c Longitude of center based on Min (purple), CM0 (yellow) and CM1 (turquoise). d Latitude of center based on Min (purple), CM0 (yellow) and CM1 (turquoise). Vertical dashed lines highlight special events of SAA area decrease (b), SAA center eastward drift (c) and SAA center rapid southward drift (d)

Figure 4 also shows the results for the ensemble of all 100 realizations of COV-OBS.x1 (light colors). For all quantities, the envelopes around the mean values are rather thin at all times, albeit slightly thicker at early periods. Clearly the SAA, being a surface property, is weakly sensitive to the small-scale field. We therefore conclude that the results in Fig. 4 are robust and insensitive to the field model realization.

Table 1 presents the mean rates of change of the SAA area and coordinates of center based on the various models. These mean rates of change correspond to the mean slopes of the corresponding quantities plotted in Fig. 4b–d. More specifically, in Table 1 we compare the mean rates of changes for the periods when the above mentioned special events were captured by our S1 and CM1 preferred models vs. the more ’typical’ periods, i.e. when the SAA area increased and its center moved mostly westward with little latitudinal mobility. Our S1 model contains a period of $\sim 50$ years in which the SAA area was nearly flat. Moreover, the total rate of change of our S1 model is about $30\%$ lower than that of the commonly used S0, demonstrating the contribution of the global surface intensity decrease to the apparent evolution of the SAA area based on the latter. The total westward drift of model Min is about twice larger than that of our CM1 model. In addition, according to CM1 the SAA drifted eastward during a period of $\sim 40$ years, whereas Min drifted westward throughout the entire period. Note that unlike the nearly flat SAA area decrease event of S1, the eastward drift event of CM1 is non-negligible, of about the same order of magnitude as its rate of westward drift over the entire period. Finally, according to model Min the SAA drifted southward monotonically and decelerated towards present day. In contrast, our model CM1 shows two periods with little latitudinal change and in between a period of $\sim 80$ years in which the SAA drifted southward in an impressive rate of 0.096$^\circ /\hbox {year}$, nearly three times faster than the average southward drift rate of Min over the entire period.

Table 1 Mean rates of change of the SAA area in $10^5$ $\hbox {km}^2/\hbox {year}$ and of the coordinates of its center in $^\circ$/year for all models

We note that the mean rates reported in Table 1 should be considered with caution. Treating the SAA as a single point and a single area is somewhat artificial in the context of core dynamics. Indeed, as we will show in the next section, the temporal evolution of the SAA is affected by the motions of multiple geomagnetic flux patches on the CMB.

Outer core kinematic interpretation

What is the kinematic origin of the special events described above? Fig. 5 shows the radial geomagnetic field and its secular variation (SV) on the CMB. To infer features that are relevant for the large-scale surface field, both quantities are truncated at spherical harmonic degree and order 5 (see, e.g. Zossi et al. 2020). To analyze the special events captured by S1 and CM1, we examine three snapshots: 1920 during the SAA steady area and rapid southward drift; 1960 during the SAA eastward drift and (again) rapid southward drift; and 2000, a ‘typical’ reference snapshot. Although the non-linear intensity kernel is not centered right below the site, in practice the kernel is located around the surface observation site (Constable and Korte 2015; Terra-Nova et al. 2017; Panovska et al. 2019). We, therefore, centered the maps on the SAA region. For comparison, we also show the corresponding maps truncated at the maximum degree and order 14 of the field model (Fig. 6).

Fig. 5

Radial geomagnetic field (left) and its secular variation (right) at the core–mantle boundary for the mean model of COV-OBS.x1 in 1920 (top), 1960 (middle) and 2000 (bottom). All models are expanded until spherical harmonic degree and order 5. All maps are centered at $20^\circ \hbox {W}$ $30^\circ \hbox {S}$, i.e. on the South Atlantic. Note the different scales

Fig. 6

As in Fig. 5 but expanded until spherical harmonic degree and order 14

Our below interpretations of the SV of the SAA area and center are guided by the conclusions of Amit (2014): Correlation/anti-correlation between a radial field structure (or flux patch) with an SV structure indicates local intensification/weakening respectively, whereas coincidence of a flux patch with a center of a pair of opposite-sign SV structures suggests local drift. Following Terra-Nova et al. (2017), we focus on the main flux patches of both polarities below the SAA region. Synthetic tests demonstrate that weak surface field tends to reside near RFPs and away from NFPs (Terra-Nova et al. 2017, 2019).

The event of steady SAA area (based on S1) is related to the SV of the dominating RFPs on the CMB. In 1960 and 2000, the dominant RFP below south of Africa coincides with a same-sign SV structure (Fig. 5 middle and bottom), corresponding to local intensification, hence the ‘typical’ SAA area decrease. In contrast, in 1920, the dominant RFP below Patagonia coincides with a positive (i.e. opposite-sign) SV structure (Fig. 5, top), corresponding to local weakening, hence opposing the SAA area decrease and leading to the steady event.

The SAA eastward drift event (based on CM1) can be explained by the SV below mid-Atlantic between the Patagonia and Africa RFPs. In 1960 a southwest positive SV intrusion extends through mid-Atlantic until the southern tip of Patagonia (Fig. 5, middle), weakening the reversed flux below mid-atlantic. This period marks a transition between the dominant Patagonia RFP in the west Atlantic beforehand (Fig. 5, top) to the dominance of the Africa RFP in the east Atlantic later on (Fig. 5, bottom). The outcome of this transitional period is a brief eastward drift of the SAA.

The SAA rapid southward drift event (again based on CM1) is related to the SV of the high-latitude NFP below Antarctica during this period (Fig. 5, top and middle). In 1920 and 1960, this NFP drifted across Antarctica towards the Indian Ocean. Because this NFP is located south of the SAA, its drift away from the South Atlantic led to the rapid southward drift of the SAA. In contrast, in 2000 the SV below this NFP significantly faded (see SV scale in Fig. 5, bottom), resulting in the weak latitudinal motion of the SAA in 2000.

Finding the kinematic origins of the SAA SV in the more detailed maps expanded until spherical harmonic degree and order 14 (Fig. 6) is clearly more challenging. Nevertheless, some of the morphological relations between the radial field and its SV that we identified as the kinematic origins of the special SAA events based on the large-scale maps in Fig. 5 can also be detected in the small-scale counterpart maps in Fig. 6. These include the transition from a dominant RFP below Patagonia in 1920 (Figs. 5, 6, top) to the emergence of a dominant RFP below Africa (Figs. 5, 6, bottom). Another example is the dissipation of the NFP below Antarctica (Fig. 6) (see also Terra-Nova et al. 2017).

There are two main differences between our interpretation of the SAA motion to that of Terra-Nova et al. (2017). First, we consider the CM1 model based on the center of mass of the area factored by the time-dependent mean surface intensity outside the SAA, whereas Terra-Nova et al. (2017) tracked the intensity minimum Min. Second, we analyzed the large-scale field and SV on the CMB which are in general appropriate for any surface application (Zossi et al. 2020), whereas Terra-Nova et al. (2017) explored the full field expanded until degree and order 14. Despite these differences, our results are in decent agreement with those of Terra-Nova et al. (2017), essentially pointing to the motions of the major RFPs and the high-latitude NFP below the South Atlantic region as the dominating agents controlling the SAA motion, in particular its deviations from linearity.

Conclusions

We introduced simple new measures to characterize the SAA. Our area calculation accounts for temporal changes in the surface intensity away from the SAA, thus the resulting SAA area S1 isolates regional morphological variations. Our center calculation is regional (rather than local), thus the resulting SAA center CM1 integrates the effects of SAA anisotropy.

As in previous studies, we find that the SAA has overall been expanding and drifting westward and southward. However, we identified periods with exceptions to the SAA ’typical’ area increase, westward drift and weak latitudinal change. These special events are non-detectable in the previous characterizations, highlighting the strongly time-dependent nature of the SAA. The special events and their kinematic origins are:

• 1890–1940: The SAA area was steady due to weakening of the Patagonia RFP.

• 1940–1980: The SAA center drifted eastward due to transition from early dominance of the RFP below Patagonia at its western limb to later dominance of the RFP below Africa at its eastern limb.

• 1900–1980: The SAA center drifted southward rapidly due to the drift of the high-latitude NFP below Antarctica away from the South Atlantic region.

It would be interesting to apply our characterization to archeomagnetic field models in order to find whether similar behavior persists over millennial timescales, bearing in mind the uncertainties in these field models (e.g. Constable and Korte 2015). This characterization may be used to constrain Earth-like numerical dynamos (Christensen et al. 2010; Davies and Constable 2014; Gastine et al. 2020), although these models operate in a non-realistic parameter space (e.g. Glatzmaier 2002). Continuous monitoring of Earth’s geomagnetic field using surface observatories and dedicated satellite mission (such as the current Swarm constellation) will reveal whether the characterization obtained in this study persists in the future.