Computing main-field models derived from MAGSAT and Ørsted satellite magnetic measurements, the crustal influence on satellite data can be treated as random noise. Satellite data can thus be used in conjunction with magnetic observatory measurements to isolate the non-core field at the observatory locations. Crustal biases for the horizontal northward X, eastward Y and vertical downward Z components are computed for all magnetic observatories where data are available for MAGSAT (1979–1980) and Ørsted (1999–2000) epochs, to study their correlation over twenty years. For a set of observatories installed after 1979 new crustal biases are computed.
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 For determining the temporal variation of the internal field, measurements from magnetic observatories remain the most useful source of information. The use of observatory data in main-field modeling needs the crustal magnetic field contribution be taken into account. This is also true when using combined satellite and ground datasets. Omitting the crustal biases in modeling can lead to local errors of about 2000 nT (about 10% of the total field over some areas), affecting the large scales of the field (in the spherical harmonic analysis truncation). One method to avoid these artifacts is to use only the time derivative of the observatory measurements, i.e. the secular variation, the main field being derived from the satellite dataset [Cain et al., 1983]. Applying this method, the ionospheric field contribution can not be estimated (simultaneous ground and satellite measurements are needed [Langel et al., 1996]). Another method is to take into account the crustal magnetic biases, by solving them together with the Gauss coefficients [Sabaka et al., 2001], or by computing and removing the a priori known crustal biases from the magnetic observatory measurements. The crustal biases are estimated by comparing the magnetic components measured in an observatory with those predicted by a geomagnetic model, truncated to its nuclear part (i.e., up to degree and order 13, based on the energy spectrum of the field [Langel and Estes, 1982]). The differences are considered as the signature of the crustal field with an induced or remanent origin. These short wavelength biases characterize the observatory area [Langel et al., 1982; Gubbins and Bloxham, 1985; Langel and Estes, 1985; Bloxham and Gubbins, 1986]. The accurate determination of the observatory location is crucial, as well as the quality of the measurements. [Langel et al., 1982] noted that the biases can be partly related to a poor knowledge of the position of the observatory, or to some problems linked to measurements.
 Some sets of crustal biases have been published, using MAGSAT data to model the geomagnetic field. These crustal bias sets have been computed using two slightly different approaches. The first one is a direct method: the observatory biases are the differences between the observatory annual mean values and the values predicted by a model computed only from satellite data, for the same spatial and temporal parameters [Barraclough, 1985; Gubbins and Bloxham, 1985; Bloxham and Gubbins, 1986; Jackson, 1989; Ultré-Guérard, 1996]. In this method the main-field model based on satellite data is assumed not to be affected by the local crustal biases. The second method is an inverse one: the crustal biases are considered as unknowns in inverting jointly satellite and observatory data [Langel et al., 1982; Langel and Estes, 1985]. The observatory crustal bias is then the constant, non-modeled part of the observatory magnetic field measurement.
 In this study we compare the crustal biases computed for the MAGSAT epoch with new crustal biases re-evaluated using Ørsted-based models. We also compute the crustal biases for some new observatories installed after 1979.
2. Method and Data
 We consider that the internal field at a given observatory location can be represented as the vector sum:
where is the main (core) field and is the crustal bias which may change appreciably over a distance of a few km.
 At the satellite altitude, the magnetic signature of the short wavelength of lithospheric origin can be considered as a random noise with respect to the large wavelength of the core magnetic field . In this study we consider the satellite data free from the effects of the crustal fields and thereafter the biases (Xc, Yc, Zc) are computed as differences between the magnetic components (Xi, Yi, Zi) measured at the observatory and the components (Xm, Ym, Zm) predicted by a model based on satellite data.
 The method is applied for two-month satellite datasets: November and December 1979 for MAGSAT and November and December 1999 for Ørsted. The two-month period is chosen as a reasonable compromise between modeling errors due to an uneven geographical coverage [Langlais and Mandea, 2000] and errors due to the secular variation [Langel and Estes, 1985]. Moreover, considering the same period of the year it is not necessary to take into account the annual and semi-annual external variations. Main-field models are denoted as M19791112 and Ø19991112 as described in [Langlais et al., 2002]. Noting t the associated time in hour of a satellite measurement, the selection criteria were Kp(t) ≤ 1+, Kp(t ± 3) ≤ 2−, |Dst| ≤ 5 nT, |d(Dst)/dt| ≤ 3 nT.hour−1. Only night time data were kept (0600 LT for MAGSAT, 2200 LT for Ørsted). Finally, data were sorted to get their geographical distribution as equiangular as possible.
 Observatory daily mean values, for all three components and available over the same two months as the satellite data, were obtained from the WDC - Copenhagen, Denmark, or directly from the observatories. All data have been screened to assert their validity. We checked the consistency of data [Alexandrescu, 1998] using the available daily or monthly mean values over the 1979–1999 period. This revealed that in some observatories changes in the baseline levels occurred between 1979 and 1999, and they were applied. All daily mean values were then averaged to obtain two-month mean values for the epochs 1979.92 and 1999.92.
 Crustal magnetic field may be of induced or remanent origin. We here assume a purely remanent field, which is expected to be constant over time. Magnetic crustal biases computed from two independent satellite-based models should thus be equivalent. However, accurate determination of the crustal biases highly relies on the capability of the model to well describe the main magnetic field. Two distinct main-field models, for two different epochs, computed with the same parameters ensure a more credible estimation and comparison of the crustal biases.
 We first compare the observatory magnetic biases published by different authors [Langel et al., 1982; Barraclough, 1985; Gubbins and Bloxham, 1985; Langel and Estes, 1985; Bloxham and Gubbins, 1986; Langel, 1987; Jackson, 1989; Ultré-Guérard, 1996] with the biases computed in this study. Only 30 observatories are common to all. Figure 1 shows this comparison: for each observatory and component, the minimum, maximum and mean crustal biases are plotted, together with the value computed in this study, based on the MAGSAT model. The rms and the correlation coefficients between previously computed crustal biases and those computed in this study for the MAGSAT epoch are presented in Table 1. Except for a few differences (FCC for Xc, CMO for Yc, CMO and VIC for Zc), all our estimations are within the interval delimited by the minimum and maximum previous computed biases. It is also worth noting that these intervals may be large, as for ABG, ANN and FCC for Xc, and for ABG, ANN and FRD for Zc (≃200 nT). The observed differences may be related to the different methods used by the authors. Another explanation may be the change in the observatory position, or the use of different coordinates. For example, the location of GDH observatory (not shown on Figure 1) changed of a few tens of kilometers in 1976. Some authors computed the crustal biases for the first site [Langel et al., 1982; Gubbins and Bloxham, 1985], some others for the second [Jackson, 1989; Ultré-Guérard, 1996]. We strongly recommend that crustal biases are published with the coordinates used.
 A more interesting result is obtained when computing the crustal biases for the MAGSAT and Ørsted epochs. We consider 62 observatories for which data are available for both epochs (Table 2). Correlations between the biases computed for each magnetic component are presented in Table 3. The obtained crustal biases for 1979 and 1999 are as close as 20 nT for 85% of the observatories. Considering CLF observatory, for which the changes in the magnetic environment are well-known by us, the differences between the crustal biases are 0, −6, 5 nT, infor the Xc, Yc, Zc. The largest differences are 49 nT in Xc (AAA), 46 nT in Yc (DRV) and 58 nT in Zc (SBA). These differences may be related to the external magnetic perturbations as the two epochs (1979.92 and 1999.92) are near the solar maximum: the averaged ap indices are 10 and 9 in November and December 1979, compared with 14 and 10 in 1999; mean Dst values over these periods are −7 and −13 nT, corresponding to changes in the magnetic field of about 1–2 nT.
Table 2. Observatories Considered in the Present Study
Considered ranges: (1) all, (2) ±500 nT, (3) ±200 nT, (4) ±100 nT.
Number of observatories within the range.
rms misfits in nT.
 Finally, we compute the crustal magnetic biases for the observatories installed between 1979 and 1999. These new crustal biases are presented in Table 4. Some of these observatories are crucial in main-field modeling, as they are located in regions with a paucity of observatories (AMS, CTA, SPT). Furthermore, some biases are very large, and their omission could lead to large modeling errors.
Table 4. New Observatories Considered in the Present Study
Longitude of the observatory, in degrees, positive eastward.
Crustal biases, in nT.
 Detailed studies of the crustal biases are important when observatory data are used in geomagnetic field modeling. Thus it is important to remove these crustal biases from the observatory data to avoid modeling errors when using combined observatory and satellite datasets. In this study we compute the observatory crustal biases a posteriori the model generation. Our comparison of published crustal biases indicates that the crustal field is larger in Z than in the other elements. Not surprisingly, the most important differences between the biases previously published are found for this component. This could be the signature of induced field. However, when analyzing the bias evolution versus the field evolution or the magnetic latitude, no clear relationship is found.
 The new biases computed using the Ørsted model are very close to the ones computed with the MAGSAT model, supporting the idea that the crustal field did not change over the last twenty years. Clearly the computation of crustal biases relies not only on the observatory measurement quality but on the quality of the satellite-based model.
 A possible improvement in estimating the crustal biases is the use of “quiet” monthly means, i.e. based on the five quietest days per month. Such dataset would help in separation of induced and remanent contributions. This test requires more work in obtaining the data from observatories, and will be the subject of further study.
 The authors would like to thank the stuff of the geomagnetic observatories for their kind supplying of high-quality data. The Ørsted satellite is funded by the Danish Ministry of Transport, the Ministry of Research and Information Technology and the Ministry of Trade and Industry. Additional support was provided by the National Aeronautics and Space Administration, the European Space Agency, Centre National d'Etudes Spatiales and Deutsche Agentur Für Raumfahrtangelegenheiten. This is IPGP contribution number 1836.