## 5 Discussion and Conclusions
The main limitation concerning the ground motion component is associated with the short duration of the present EGMS dataset, but the yearly updates that are foreseen will alleviate this restriction; having longer time series will be of help in understanding whether it is reasonable to extrapolate the present rates into the future. Recently, the dataset was extended to 2021, so the estimates of vertical ground displacement are now based on 6 years (2016 to 2021). This is a small step forward compared to the analyses we recently presented [120] for different study areas by using the same methodological approach. However, it should be noted that a European product validated by Copernicus \begin{table}
\begin{tabular}{l c c c c} \hline \hline  & **Marina di Campo** & \multicolumn{2}{c}{**Fertilia**} \\ \hline  & **SLR (cm)** & **SUSL (km\({}^{2}\))** & **SLR (cm)** & **SUSL (km\({}^{2}\))** \\ \hline Rahmstorf 2007 * & 143.2 & 0.39 & 145.2 & 2.29 \\ IPCC 2013 * & 102.2 & 0.14 & 102.2 & 1.89 \\ MED16 2022 ** & 58.3 & 0.09 & 62.6 & 1.44 \\ \hline \hline \end{tabular}
\end{table} 
Table 6: Comparison of terrain under sea level (km\({}^{2}\)) in 2100 predicted by using previous scenarios ([PERSON], 2007 [117] and IPCC, 2013 [118]; [PERSON] et al., 2020 * [25]) and Med 16 Model of [PERSON] et al. (2022 [72]; present study **). is already a great step forward, and this product will be further improved when data from the most recent satellite constellations will be available [121; 122]. Figure 14: Comparison of different inundation models using the projection of Rahmstorf 2007 [114] *, IPCC 2013 * [25] and Med 16 [72] **; present study). The SLR used for the projection is reported close to the colour bar (cm). We tested our new methodology on coastal areas that were recently indicated as nearly stable ones [123], where we may expect that EGMS trends are more reliable. A recent investigation [124] has shown that in the Pontina coastal plain there is very close agreement between the EGMS dataset and geological records from the MIS 5.5 (Tyrrhenian), and this result is in agreement with other studies [123; 124; 125; 126]. For other areas, we are already processing multisource data in order to verify the congruency between long-term geological data and short-term remote sensing data. Clearly, there are also unstable coastal regions, such as Campi Flegrei and Calabria, where the analysis should be complemented with detailed in situ measurements. It should be noted that in the central Mediterranean area, and particularly in Italy, vertical movements due to volcanism, tectonics, and isostasy can be calculated using geological and instrumental methods [16; 17; 18; 19]. The maximum highstand of MIS 5.5, which occurred 118 thousand years ago, is the most used geological method, and many scientific papers and databases about Italy are available in the literature [17; 123; 3; 127]. The rates coming out from those geological markers range from +1.7 to \(-\)1.2 mm/year [128]. The geological markers are very useful because they average, for the past 118 thousand years, the result from different movements, including co-seismic ones from earthquakes, with the recurring event time of 50-100 years. The vertical movements, due to glacio-hydro isostasy (GIA) are well known and modelled for the central Mediterranean area, showing values from \(-\)0.1 to 0.6 mm/year [17; 22]; in Northern Europe (Norway, Sweden, and Finland), instead, higher values are recorded with an uplift rate larger than 1 cm/year. Moreover, some other vertical movements could happen, caused by subsidence, uplift, and proximity to volcanoes or eruptive sites. As an example, the area belonging to the town of Venice, Italy, has experienced a relative sea level rise of 25.3 cm in the past hundred years in contrast to the rate of 13.1 in other stable areas of the Mediterranean Sea [16; 18; 30]. Another source of uncertainty is related to the accuracy of the SLR modelling estimates.