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The accuracy, density and distribution of gravity data used in the geoid determination are the factors that affect the accuracy of the geoid. The observation of the gravity is easy and cheap on land relatively, but requires great effort, time and cost in sea. Therefore, the accuracy of the geoid at shore regions of which the gravity data distribution and density are insufficient is low before the altimetry satellites. By means of the altimetry satellites, it becomes possible to derive gravity from altimetry observations. Altimetry satellites basically determine the distance between the satellite and a target surface (oceans) by measuring the trip time of a radar pulse moving among the satellite and ocean. To do this, the altimeter emits a radar wave and analyses the return signal. The Sea Surface Height (SSH) which altimeter measure is the height difference between the satellite's height with respect to a reference ellipsoid and the satellite-to-ocean surface distance (calculated by measuring the time taken for the signal to make the round trip). On the other hand, altimeters can measure wave height, wind speed, rain rate over the oceans and detection of crevasses over ice shelves besides the surface height. The measured SSH can be transformed into gravity anomalies and deflections of the vertical by using the Brun's formula. The lack of gravity data is satisfied by the altimetry derived gravity data. Since the economical value and high population density of the shore regions, density and importance of the engineering applications are great in these regions. Determining an accurate geoid by using altimetry derived gravity data, has not only scientific importance but also economical importance since it is a geodetic infrastructure. In this study, the possibility of determining accurate gravity field, geoid and finally the sea surface topography is investigated. Approximately fifteen-year data from TOPEX/POSEIDON, GFO, ENVISAT and GFO satellite altimetry missions are used for the recovery of gravity anomalies over the Eastern Mediterranean Sea (region between the longitudes of 28°-36° and latitudes of 32°-37°). The Corrected Sea Surface Height (CORSSH) data used in calculations which are received as corrected for all standard errors from DGFI (Deutsches Geodätisches Forschungsinstitut). Least Squares Collocation (LSC) method and remove restore technique are used to derive gravity anomaly from SSH and geoid from gravity anomaly. The EGM08 geopotential model is used as the reference geopotential model during the remove restore step. Model covariance functions consistent with the empirical covariance functions are determined for residual SSHs and residual gravity anomalies. The covariance function parameters are involved in LSC calculations. The GRAVSOFT package software is used in calculations and the Generic Mapping Tools (GMT) software is used in drawings. The gravity anomaly field calculated in this study is compared to the Smith Sandwell 97, KMS02 and DNSC08 global gravity anomaly models. Since the altimetry observations degrade at the coastal regions, altimetry derived gravity field also degrades at the coastal regions. So the comparison is carried out at the points that are 30 km ore more far from the shore line. According to comparison results, the gravity anomaly model which is calculated in this study is found to be consistent with the Smith Sandwell 97, KMS02 and DNSC08 models within the range of ± 2.54 mgal, ± 3.52 mgal and ± 1.49 mgal respectively. The calculated gravity anomaly field is also compared to the ship observations. According to calculation results, a consistency of ± 7.96 mgal is found between the ship observations derived gravity anomaly. The geoid heights calculated from gravity anomalies are compared to the TG03 Turkish Geoid and a consistency of ± 0.52 m is found. After calculating the geoid heights, the Sea Surface Topography (SST) is determined. The calculated SST model is compared to the DNSC08 SST model and a consistency of ± 0.09 m is found between these models. It can be said that by using the altimetry data it is possible to determine a gravity field within the accuracy of ± 8 mgal Also it is obvious that altimetry data improves the geoid quite significantly at coastal regions. It is expected that more accurate results can be obtained by combining altimetry derived gravity anomalies with land, aerial and ship gravity observations. [ABSTRACT FROM AUTHOR]