Our aim is to assess the range and the characteristics of radial orbit errors on regional and global scales. Therefore, the differences between three independent state-of-the-art orbit solutions available for the TOPEX/Poseidon mission are analysed. All orbit solutions are derived in the International Terrestrial Reference Frame (ITRF) 2008 (Altamimi et al., 2011) and use satellite laser ranging (SLR) and Doppler Orbitography and Radiopositioning Integrated by Satellite (DORIS) tracking data but are based on different software and on distinct models. The actual multi-mission GFZ orbit solution VER11 (Rudenko et al., 2017) is used as a reference in this paper and is called REF hereafter. The GSFC std1504 orbit (Lemoine et al., 2010; Beckley et al., 2015) has been chosen by the ESA CCI Sea Level Phase 2 project and differs in many aspects from the GFZ orbit, regarding software as well as the suite of implemented models including another Earth's gravity field model. As the third model, we have chosen the GRGS orbit solution (Soudarin et al., 2016), which is derived using models similar to those of the GFZ solution but employs another software package. The main models used for GFZ REF, GRGS, and GSFC std1504 orbits are described in Table 1. The main differences in these three orbit solutions are related to the choice of the Earth's time-variable gravity (TVG) field models, ocean tide model, modelling of non-tidal atmospheric and oceanic gravity, and the treatment of geocentre variations in station displacements, as well as the constraints of the observation data (SLR/DORIS). While for the GRGS solution comparatively high weight is on the SLR data, for the GFZ solution there is higher weight on the DORIS data. Proper modelling of the Earth's gravity field, in particular of its time-variable part, is crucial for the computation of precise orbits of altimetry satellites and has been shown to contribute to errors in regional sea level trends and seasonal signals (Rudenko et al., 2014; Esselborn et al., 2015). For the pre-GRACE (Gravity Recovery and Climate Experiment) period, the TVG field is poorly constrained. The weekly TVG solutions used for the GSFC orbit were derived up to degree and order 5 from the analysis of SLR and DORIS observations to 20 geodetic satellites starting from 1993 (Lemoine et al., 2016). The TVG part used for the GFZ REF (GRGS) orbits consists of the combination of yearly coefficients, drift terms, and annual and semi-annual variations for degrees and orders 1 to 80 (2 to 50) derived from GRACE data and SLR measurements to the Laser Geodynamic Satellite (LAGEOS)-1/2. The annual and semi-annual coefficients used for the GFZ REF orbit are fitted yearly starting from August 2002. For the pre-GRACE period before August 2002 (January 2003), only the degree-2 terms exhibit yearly values and drift terms; however, the annual and semi-annual variations, which were derived for the GRACE period, are applied for degrees and orders 1–80 (2–50) (Rudenko et al., 2014, Förste et al., 2016).

The approach adopted for the estimation of the radial orbit errors implies that errors common to all three orbits cannot be detected. In particular, all three orbits rely on the ITRF2008 reference frame and basically the same set of tracking stations. To further estimate the orbit-related radial orbit error budget due to the most significant factors, we have derived five test orbits based on the GFZ REF orbit. The errors related to inconsistencies of the tracking data networks are tested by using only one tracking network instead of two. Since the GRGS orbit was derived without estimation of the DORIS system time bias, we have studied the impact of this bias on the radial orbit differences with special focus on systematic differences between ascending and descending passes. The effect of errors in the realization of the terrestrial reference frame is tested by the implementation of the most recent ITRF2014 version. The effects of uncertainties in Earth's TVG field models are tested by the implementation of the EIGEN-6S2 model which is the predecessor of the EIGEN-6S4 model. For each case, the same background models and estimated parameters were used as for the REF orbit, except for those that represent the changes for the specific test case. The five test orbits and the differences with respect to the GFZ REF orbit are

SLR orbit: derived by using SLR tracking observations only;

In order to assess the orbit accuracy at crossover points and to relate the estimated errors to the total variability of the sea level data, along-track TOPEX Sea Level v1.1 Essential Climate Variable (ECV) data (Ablain et al., 2015) released from the ESA CCI Sea Level project have been included in the analyses. The along-track data have been corrected for all instrumental and geophysical effects by the state-of-the-art models provided with the data. However, for some corrections, updated models were applied. These include EOT11a ocean tides and loading tides (Savcenko and Bosch, 2012), solid Earth tides following the International Earth Rotation and Reference Systems Service (IERS) 2003 Conventions, and updated GPD+ wet tropospheric corrections (Fernandes and Lazaro, 2016). The altimeter crossover differences were calculated for each test orbit separately. For the calculation of sea level anomaly grids, the GSFC std1504 orbits have been selected. The processing of the data, the crossover point analyses, and collinear analyses, as well as the interpolation to a regular grid, were performed using GFZ's Altimeter Database and Processing System (ADS) Central (Schöne et al., 2010).

In the following, the performance of the analysed orbits is evaluated. For the GFZ orbit solutions, the consistency with tracking data and at arc overlaps is assessed. Table 2 provides the main results of precise orbit determination of the GFZ reference and test orbits, namely, the average values of SLR and DORIS root mean square (rms) fits; radial, cross-track, and along-track 2-day arc overlaps, illustrating the internal orbit consistency in these directions; and the number of the arcs used to compute these values for the reference and five test orbits. When using the same observation types and weighting, smaller values of arc overlaps and observation fits indicate improved orbit quality. Reduced radial arc overlaps characterize reduced radial orbit error. SLR observations were used at all 494 orbital arcs of five GFZ orbits, except for the DORIS orbit for which no SLR observations were used at all. Since DORIS data are available for TOPEX/Poseidon only until 31 October 2004, these data were used at 459 orbital arcs preceding this date, except for the SLR orbit for which no DORIS observations were used at all. All orbital arcs for GFZ orbits are manoeuvre free. Thus, 2-day arc overlaps were computed for 433 overlaps for the REF, TBias, ITRF14, and Geoid orbits. In the case of the SLR and DORIS orbits, a few gaps in the observations caused radial arc overlap larger than 0.5 m. Those arc overlaps have been excluded from the statistics resulting in fewer arc overlaps shown for these orbits in Table 2.

Figure 1 provides information on the SLR rms fit of the reference and tests orbits, while Fig. 2 displays the radial arc overlap of two consecutive 2-day orbit arcs. The four orbits derived using SLR and DORIS observations provide comparable levels of average SLR rms fits (1.96–1.99 cm; Fig. 1). The smallest SLR rms fit (1.59 cm) but largest radial arc overlap (1.72 cm) are obtained for the SLR-only orbit, indicating a weak orbit quality over large geographical areas. The largest SLR rms fit is obtained for the TBias orbit. When no DORIS system time bias is estimated, inconsistencies between the timing of the observation system result in higher misfits. Among the five orbits derived using DORIS observations, a slightly increased average value of the DORIS rms fits (0.04795 cm s-1) is obtained for the DORIS orbit derived using only DORIS observations (related to the weighting of observation types and the number of observations used) followed by the TBias orbit (0.04785 cm s-1), while the other orbits derived using SLR and DORIS observations (REF, ITRF14, and Geoid) show comparable average values of the DORIS rms fits (0.04775–0.04778 cm s-1). The smallest average value of the radial arc overlaps (Fig. 2) is obtained using the EIGEN-6S2 geopotential model (0.83 cm). The radial arc overlaps of the TOPEX/Poseidon orbit derived using only SLR data are 1.95 times larger than those of the orbit derived using only DORIS data. Using the reference frame ITRF2014 instead of ITRF2008 eliminates many outliers in the radial arc overlaps and therefore reduces the average value of the radial overlaps from 0.90 to 0.84 cm.

The DORIS system time bias is regularly estimated and applied during GFZ's POD process to adjust the DORIS time system to the SLR time system. Zelensky et al. (2006) showed that there is a strong linear relationship between along-track orbit position and the DORIS time bias. The comparison of the fits and overlap values of the REF and the TBias orbits (Table 2) shows that the estimation of the DORIS time bias improves the orbit quality. The temporal behaviour of the DORIS system time bias derived for the TOPEX/Poseidon REF, ITRF14, and Geoid test orbits is in close agreement (Fig. A1) and resembles the estimation given by Lemoine et al. (2016). For the GFZ VER11 (REF) orbit, it indicates variations between -22.4 µs and +4.4 µs from 1992.73 to 1994.18, followed by a period of a linear trend of 35.11 µs yr-1 between 1994.18 and 1995.00 that ends with a jump from -28.65 to +1.98 µs around 1995.00. Then, the DORIS time bias shows two rather stable periods with a mean value of +3.70 µs with a standard deviation of 1.77 µs from 1995.0 to 1999.0 and a mean value of -1.32 µs with a standard deviation of 1.19 µs from 1999.0 to 2001.13, followed again by a period of a linear trend (-3.14 µs yr-1) from 2001.13 to 2004.83. The mean value of the DORIS system time bias is 0.04 ± 0.36 µs for the DORIS test orbit, and it is equal to zero (not shown in the figure) for the TBias orbit.

For all orbit solutions, a crossover point analysis for the period April 1993 to September 2004 has been performed based on the altimeter data described in Sect. 2.2. Differences between the values of ascending and descending passes at crossover points are caused by oceanic variability and errors related to the measurements, the orbit, and the applied corrections. Since in our study errors related to the measurements and the applied corrections and oceanic variability are always identical, here, smaller absolute median differences and decreased rms values at crossover points are indicative of increased orbit quality. The median of the time series of global mean height differences and rms values at the crossover points are provided in Table 3. The smallest ascending/descending differences (-1.6 mm) and as well the lowest rms values (49.5 mm) at the crossover points are reached by the GSFC orbit solution. The median global ascending/descending differences are -3.1 mm for the GFZ REF and -3.0 mm for the GRGS orbit solutions. However, while the rms value of the GFZ REF solution (49.8 mm) is comparable to the one of the GSFC (49.5 mm), the GRGS orbit solution shows degraded performance (51.3 mm rms). Keeping the DORIS time bias fixed to zero deteriorates the median differences between ascending and descending passes to -3.6 mm but does not change the rms value. The median of the global mean ascending/descending differences is -2.7 mm for the SLR and -4.7 mm for the DORIS orbits. Both orbit solutions show degraded performance (51.2/50.7 mm rms) with respect to the REF solution. This shows that using SLR and DORIS observations together improves the orbit quality considerably, even though the DORIS observations seem to aggravate the mean differences between ascending and descending tracks. Using ITRF2014 instead of ITRF2008 does not change the rms of crossover differences but improves their median values. The Geoid orbit solution exhibits clearly improved ascending/descending differences (-2.1 mm) as well as a slight reduction of the rms values. A further analysis of the temporal evolution of the ascending/descending differences reveals that these improvements take place in the pre-GRACE period before August 2002.

In order to estimate the orbit-related errors in sea level height, the differences between the radial components of the GFZ REF orbit and the two independent orbit solutions (GSFC and GRGS) have been analysed. To assess the effect of uncertainties in the reference system, in the realization of the tracking station networks and in Earth's time-variable gravity on the radial error budget, we have evaluated the differences of the radial orbit components between the GFZ's REF and ITRF14, SLR, DORIS, and Geoid test orbits. Since the radial orbit components map directly to the derived sea level heights, we consider the differences presented here to represent estimates of the orbit-related sea level error. However, since the orbit error analysis is based on orbit differences, any error common to all three orbits will be lacking in our assessment.

The differences of the radial orbit components at the time of the altimetry measurement (1 Hz, ∼ 6.7 km on the ground) are calculated and interpolated to a global 1∘ × 1∘ grid for every cycle (9.92 days). In general, we merge both ascending and descending passes in our calculations. In addition, we analyse ascending and descending passes for some orbit combinations separately. In order to study the global mean differences between the radial orbit components and their temporal evolution, global mean rms values per cycle are derived. They are calculated as the square root of the spatial weighted mean of all squared radial orbit differences on the 1∘ × 1∘ grid for the respective cycle.

Since we are not interested in the orbit error itself, but rather in the effect of radial orbit errors on global and regional sea level, we treat the radial orbit differences the same way as the sea level values from altimetry. For the estimation of global mean errors, the gridded radial orbit differences are averaged (with area weighting) over the ocean (±67∘ latitude). Starting from these global mean orbit differences, global mean rms values relative to the temporal mean of the series are calculated as an estimate for the orbit-related error of the global mean sea level. Decadal trends, annual and semi-annual signals, and the corresponding formal errors are estimated by a least-square fit. The seasonal errors are derived from the amplitudes of the annual signal. As a measure of errors at interannual timescales, we calculate the rms of the 5-year running trend series of the radial orbit differences. Since the time series is only 11 years long, it is not possible to derive statistically sound estimates of the decadal trend. Here, the errors of decadal trends are assumed to correspond to the absolute values of the trends fitted to the series of the radial orbit differences. For the estimation of regional upper bound errors, at each grid point, rms values relative to the local temporal mean, annual cycle, rms of the 5-year running trend, and decadal trends are calculated in correspondence to the global analyses. From the 1∘ × 1∘ grid, the maximum values over the ocean are extracted to estimate regional upper bound errors.

In order to relate the estimated errors to the total variability of the sea level data, TOPEX altimeter data have been included as well. The data and the processing are described in Sect. 2.2. From the gridded sea level anomalies, seasonal, interannual, and decadal trends were derived using the methods described above.

In the following, we investigate the orbit-related global sea level error, differentiating between the total error and its annual, interannual, and decadal components. The TBias orbit differences are not included in these analyses but will be further investigated for the study of changes between ascending and descending passes (Sect. 3.4). The time series of the global mean rms of gridded radial orbit differences per cycle are shown in Fig. 3 for all orbit solutions relative to GFZ's REF orbit. The largest differences occur between the REF and the GRGS orbits; the smallest changes occur for the ITRF14 test orbit. Most orbit differences are dominated by subseasonal variability; only for the Geoid and ITRF14 orbits the rms per cycle series are governed by seasonal and decadal periods. For the Geoid, GSFC, and GRGS orbit differences relative to the REF orbit, the rms series exhibit a seasonal cycle, which is an indication for seasonal orbit differences on regional scales. The rms of the REF minus Geoid orbit difference is decreased after August 2002, indicating that the main differences between the two orbits originate from the pre-GRACE period. In contrast, the differences between the REF and the ITRF14 orbits slightly increase from 2000 onwards.

From the time series of global mean orbit differences over the oceans, the rms, annual cycle, 5-year trend variability, and decadal trend differences are calculated and used as an estimate of the orbit-related error on different timescales. These orbit errors are summarized in Table 4 for all orbit models together with the corresponding values derived from altimetric sea level anomalies. The global mean rms of the radial orbit differences between the REF and GRGS (GSFC) orbits amounts to 1.2 (1.1) mm, which corresponds to 8 % of the global mean sea level variability of 13.0 mm. The restriction to one tracking station subnetwork leads to large changes of the orbit; for the DORIS (SLR) orbit solution, the rms values of the radial differences with respect to the REF orbit amount to 1.8 mm (0.7 mm), which exceeds the size of the estimated total orbit errors. This highlights the importance of manifold, precise, and consistent tracking data for accurate global mean sea level estimates. The substitution of the Earth's gravity field model (EIGEN-6S4 by EIGEN-6S2) and the ITRF realization (ITRF2008 by ITRF2014) accounts for 0.2 and 0.3 mm, respectively, of the mean rms orbit errors. A spectral analysis of the global mean radial differences (Fig. A2) exhibits peaks at ∼ 60 days for all but the GRGS and TBias orbit differences and at ∼ 90 and ∼ 170 days for the SLR and DORIS orbit differences. An annual component can be observed for the GRGS and Geoid orbit differences. Since the annual amplitude is less than 1 mm only, it can be neglected and is not included in Table 4. The time series of the 5-year running trends of the global mean radial orbit differences over the ocean are shown in Fig. 4 for the various orbit combinations. All curves range between -0.3 and +0.2 mm yr-1, and show at least one zero crossing and imply interannual changes of the estimated decadal sea level trends. The corresponding curve of the 5-year running trends for the global mean sea level (not shown) ranges between 4 mm yr-1 in the year 1997 and 2.6 mm yr-1 in 2000. Before 1998, the GSFC and GFZ solutions are close to each other and both suggest smaller sea level trends for this period than the GRGS solution. After that, trends derived from GFZ orbits are weaker than the ones derived from GSFC orbits and stronger than the ones derived from GRGS. The maximum interannual trend variability of 0.1 mm yr-1 occurs between the REF and GRGS orbits (Table 4) which amounts to almost 30 % of the corresponding value derived for the global mean sea level curve (0.37 mm yr-1). An error of this size might interfere with the estimation of global mean sea level acceleration. Hence, relative to the GFZ orbits, the use of the GSFC (GRGS) orbits would result in a slightly increased (decreased) acceleration of the global mean sea level curve during the TOPEX period. Since the exclusive use of the DORIS tracking station leads to interannual trend variability of 0.11 mm yr-1, inconsistencies of the tracking stations' subnetworks might explain large portions of the observed global mean interannual variability. The errors of the interannual trend variability are for all orbit combinations higher than for the decadal trends. The global mean decadal trends (calculated over the full mission time) are mostly significant but can be further neglected, since they are well below the uncertainty of the corresponding global mean decadal sea level trend (±0.5 mm yr-1).

The maximum regional errors derived from the analysis of the gridded orbit difference series over the oceans are summarized in Table 5. The TBias orbit differences are not included in these analyses but will be further investigated for the study of changes between ascending and descending passes (Sect. 3.4). Regionally, the maximum radial orbit differences on the 1∘ × 1∘ grid between the REF and GRGS (GSFC) orbits amount to 10.7 (7.4) mm. The exclusive use of only one tracking station subnetwork leads to distinct changes with rms values of 9.3 (7.2) mm for the DORIS (SLR) subnetwork. This suggests that for the weighting factors applied with GFZ's REF orbit especially inhomogeneity in the SLR station subnetwork has the potential to produce notable regional orbit errors.

Annual difference signals with respect to the REF orbit are most prominent for the GSFC and GRGS solutions, while they are negligible for the SLR, DORIS, and ITRF14 orbits. The corresponding patterns of the annual amplitudes for the differences of REF versus GSFC, GRGS, and Geoid orbits and of GRGS versus GSFC orbits are shown in Fig. 5. The observed patterns for the GSFC and GRGS orbit differences consist of a dipole with centres in the south-eastern Indian Ocean and the Caribbean. Since the two centres are phase shifted by half a year, the effect on the global mean differences is marginal. The pattern coincides with the patterns already shown to be related to the use of AOD1B products (Rudenko et al., 2016a) and different time-variable gravity fields for TOPEX/Poseidon POD (Esselborn et al., 2015). However, the annual differences between the REF and Geoid orbits can only explain part of the observed differences between the REF and GRGS orbits. In addition, the annual differences between GRGS and GSFC orbits are quite small and show no distinct pattern. Another plausible source of the relatively strong signal for the GSFC and GRGS orbit cases is the differences in the annual corrections for station coordinates by geocentre motion corrections and non-tidal atmospheric loading. A careful consideration of the relevant models used for the POD of these three orbits suggests that the observed differences originate in part from the non-tidal atmospheric loading effect on the stations which was applied for the GFZ but not the GRGS and GSFC orbits. There is evidence that the annual signal from the EIGEN-6S2 gravity field model is closer to the gravity field solution applied for the GSFC orbits than to the one from EIGEN-6S4 – at least in the pre-GRACE period (Fig. 5).

The patterns of the interannual variability of the regional trends are shown in Fig. 6 for all orbit differences. The trend errors reach up to 1.2 (0.9) mm yr-1 for the GSFC (GRGS) orbit differences (Table 5). The patterns of the trend variability from the GSFC and GRGS differences show coinciding maxima in the regions around South America and Australia. The differences for the Geoid orbit show similar features even though the absolute trend variability is smaller (up to 0.4 mm yr-1). For the SLR and DORIS orbit differences, the patterns of interannual variability (Fig. 6) are patchy and oriented along individual tracks. For the ITRF14 solution, the trend variability is slightly increased at high latitudes (up to 0.2 mm yr-1). The patterns of the interannual trend variability derived from the GFZ test orbits suggest that differences in the TVG modelling and contributions from the tracking systems are the most plausible sources of the observed regional differences of trend variability between REF, GSFC, and GRGS orbits.

The strongest regional changes in the decadal trend (Fig. 7 and Table 5) are observed for the differences between the REF and GSFC orbits (up to 1.0 mm yr-1). For the GSFC orbit, high absolute decadal trend differences tend to coincide with maximum seasonal differences but not with maximum interannual variability. The differences between the REF and GRGS orbit trends reach 0.7 mm yr-1 at maximum, and the patterns of maximum annual amplitudes, interannual and decadal trend differences coincide. The differences between the REF and Geoid orbit trends resemble these patterns. However, the trend values are smaller (up to 0.4 mm yr-1) and can explain only about half of the observed decadal trend differences. The decadal trends related to EIGEN-6S2 and EIGEN-6S4 differences during the TOPEX period presumably originate from the modelling of the TVG after August 2002, since before drift terms are only applied to degree-2 terms. The degree-2 terms, in turn, are defined by SLR data and show close agreement between the two TVG models for the pre-GRACE period. The ITRF14 orbit differences drift locally by a rate of up to 0.2 mm yr-1 with positive values in the Southern Hemisphere and negative values in the Northern Hemisphere, indicating a drift in the z component between the reference system realizations. The observed values are in good agreement with the combined change of scale and rate of the z component of the transformation between ITRF2008 and ITRF2014 (Altamimi et al., 2016). The regional decadal trends for the SLR and DORIS orbit differences are patchy and rather related to particular tracks without consistent long-wavelength behaviour. Higher trends of up to 0.4 mm yr-1 emerge for the DORIS orbit. The patterns of the decadal trend differences derived from the GFZ test orbits suggest that differences in the TVG modelling are the most plausible source of the observed regional decadal trend differences between REF, GSFC, and GRGS orbits.

The crossover point analysis (Table 3) reveals considerable global mean differences between ascending and descending passes for most orbits. Fu and Haines (2013) showed that orbit errors might induce diverging drifts for sea level derived from ascending and descending passes. In the following, we study whether there are systematic changes to the results obtained so far when ascending and descending passes are investigated separately. Therefore, for a subset of orbit solutions, the same analyses were performed as before but for data sets derived from ascending and descending passes only. Since the DORIS orbit reveals the most pronounced median ascending/descending differences, we have chosen to study the REF minus DORIS and the REF minus TBias orbit differences further. During the POD of the GRGS orbit, the DORIS system time bias has not been estimated; therefore, we include the GRGS orbit in the analysis as well. However, in contrast to the previous analysis, we study the difference of Geoid minus GRGS instead of REF minus GRGS in order to exclude the effects of different time-variable gravity fields from the analysis.

The global mean radial orbit differences for ascending and descending passes are for all three cases in the range of ±12 mm (Fig. A3). The ascending and descending radial orbit differences are significantly anti-correlated. The correlation coefficient is almost -1 for the REF minus TBias case, almost -0.8 for the Geoid minus GRGS case, and still -0.5 for the REF minus DORIS case. The correlation is further increased for periods of more than 1 year. The REF minus TBias global mean time series resembles the DORIS system time bias applied for the REF orbit (Fig. A1). The global mean radial differences for the Geoid minus GRGS case reveal similar features as well. All three orbit differences exhibit diverging global mean radial differences for ascending and descending tracks after the year 2000. The interannual trend variability and decadal trends derived from the analysis of the global mean radial orbit difference series over the oceans are summarized in Table 6 for the merged, ascending, and descending passes. If the ascending and descending passes are analysed separately, the interannual trend variability is increased by at least 5 times for the corresponding orbit differences. Ascending passes exhibit higher variability than the descending. The differences for the global mean decadal trends between ascending and descending passes are a multiple of the values for the merged data and reach up to 0.6 mm yr-1, where both data sets are drifting in opposite directions.

The regional patterns of the decadal trend differences for ascending and descending passes are shown in Fig. 8. The DORIS orbit differences reveal a striking spread between the decadal trends of the ascending and descending passes. The trends are opposite for ascending and descending passes for most areas of the global ocean and reach regionally absolute values of up to 0.8 mm yr-1. Trends for the REF minus TBias orbit differences are very similar but smaller than the REF minus DORIS orbit ones. The corresponding analysis for the Geoid minus GRGS orbit differences shows again very similar features as for the DORIS differences. This indicates that discrepancies in the reference systems of the tracking stations (distribution of tracking stations, observation sampling, etc.) might give rise to long-wavelength orbit errors being anti-correlated for ascending and descending passes. Relevant contributions originate from uncertainties of the timing of the DORIS measurements. Increasing time biases are related to increasing along-track position errors and seem to be transferred to radial orbit errors. This mechanism is not fully understood, but a further analysis is beyond the scope of this paper. The uncertainties are especially pronounced in tropical and subtropical regions. On regional scales, the interannual and decadal trend errors derived from ascending/descending passes separately can be many times higher than the values derived from the merged data. Even though such effects tend to cancel, whenever both components are merged, they might still introduce considerable errors in regional studies that are based on along-track data, e.g. at calibration sites.

Our analysis exhibits large-scale patterns of the orbit-related error. Errors for interannual to decadal sea level trends of more than 1 mm yr-1 might hamper the interpretation of the observed sea level variability from altimetry, at least apart from the large oceanic currents. In order to define regions where the orbit-related error should be considered when analysing sea level data from TOPEX, we have determined areas with orbit errors of at least 10 % of the corresponding sea level value. Figure 9 shows the sea level variability, seasonal signal, and interannual and decadal trends derived from the ESA CCI TOPEX altimeter data for those regions where the orbit error amounts to at least 10 % of the corresponding sea level value. Taking into account the total orbit-related error, about half the ocean is affected. This includes especially calm oceanic regions, whereas for energetic regions, like the Antarctic Circumpolar Current, tropical Pacific, and the western boundary currents of the Northern Hemisphere, the dynamic ocean signal is much larger than the orbit error. For the seasonal signal, mainly the Southern Ocean is concerned. Critical regions for the estimation of the interannual variability are the tropical and subtropical Atlantic and the south-eastern Pacific. For decadal scales, the orbit-related trend errors are prominent in a couple of regions including the South Atlantic, western North Atlantic, central Pacific, and south-eastern Indian Ocean, but also several marginal seas including the Mediterranean, Red Sea, Yellow Sea, and Sea of Japan.