GRAVITY and its usage in GRAVITY interpretation is still a challenging field. It is not easy to compute these gradients especially in the case of noisy data. Analytical signal is one of the new methods that uses GRAVITY gradients to locate the perturbing body. This method had already been used for high-resolution magnetic and GRAVITY data and rarely used for low-quality GRAVITY data. The GRAVITY gradients and analytical signal have been applied in two different areas, Zahedan where we are looking for Choromite anomalies and Tehran (Mard Abad) where we are investigating for low density anomaly, Probably hydrocarbon.

A great deal of attention has been paid to quantitative interpretation in recent years Two methods, namely the analytic signal an4 the Euler deconvolution (EULDPH) were discussed in this paper. After a short review on the mathematical bases of the methods. two field examples were used to examine the efficiency and limits of the methods when they are applied on a complex geology structure. These methods have already been applied to synthetic models and high - resolution data such as gradiometeric or microGRAVITY data. Noisy GRAVITY data especially in areas of complex geology has rarely been used by these methods and the field examples are exceptions. The low- resolution GRAVITY data was used to provide with residual anomalies. GRAVITY gradients were generated ftom the residual anomaly values. Then applying the GRAVITY gradients to the analytic signal and EULDPH methods. we determine the coordinates of a perturbing body in the field of data. Two field examples, one in the west of Tehran (Mardabad) and another in the southwest of Iran are considered. In the first field we were to determine the location of a hydrocarbon density anomaly. In the second field, we were to determine a Choromit anomaly.

Euler's homogeneity equation for determining the coordinates of the source body especially to estimate the depth (EULDPH) is discussed at this paper. This method is applied to synthetic and high-resolution real data such as gradiometric or microGRAVITY data. Low-quality GRAVITY data especially in the areas with a complex geology structure has rarely been used. The Bouguer GRAVITY anomalies are computed from absolute GRAVITY data after the required corrections. Bouguer anomaly is transferred to residual GRAVITY anomaly. The GRAVITY gradients are estimated from residual anomaly values. Then by applying the GRAVITY gradients, using EULDPH, the coordinates of the perturbing body will be determined. Two field examples one in the east of Tehran (Mard Abad) where we would like to determine the location of the anomaly (hydrocarbon) and another in the south-east of Iran close to the border with Afghanestan (Nosrat Abad) where we are exploring choromit are presented.

Filariasis is a problematic tropical vector borne infection. Here, the author proposes an idea on a physical change, serum specific GRAVITY, in serum of filariasis cases and further extrapolates for its clinical usefulness. According to this study, the finalized estimated serum specificity in filariasis is more than that of normal condition. The change of the specific GRAVITY due to additional content or mass can be demonstrated and might be useful for diagnosis and following up of filariasis.

Simultaneous capillary dominated displacement of the wetting and non-wetting phases are processes of interest in many disciplines including modeling of the penetration of polluting liquids in hydrology or the secondary migration in petroleum reservoir engineering. Percolation models and in particular invasion percolation is well suited to characterize the slow immiscible displacement of two fluids when both the GRAVITY and viscous effects are negligible. In particular, the characteristic of the percolating cluster and the other important percolation properties at the breakthrough can be inferred. However, with the inclusion of the GRAVITY forces, the behavior may change. For example, as the magnitudes of the GRAVITY forces are comparable to the capillary forces, we have observed a transition in the structure of the interface (i.e. invasion front) depending on the dimensionless Bond number (i.e. ratio of GRAVITY to capillary forces).We have taken a numerical study of the displacement of two immiscible fluids in the presence of the GRAVITY force in a network of random pores. The main contribution is to investigate the effect of heterogeneity by considering various throat size distributions. We consider the injection to take place from one side of the system and displace the displaced fluid from the other side. The condition of the stability or instability of the front (or interface) is observed to be dependent on the dimensionless bond number as well as the heterogeneity of the system. 

We give in this paper an explicit construction of the covariant quantization of the rank-2 “massless” tensor field on de Sitter (dS) space (linear covariant quantum GRAVITY on a dS background). The main ingredient of the construction is an indecomposable representation of de Sitter group with different indecomposability channels. We here make the choice of a specific gauge fixing in order to get the simplest possible structure of the involved Gupta-Bleuler triplets. We describe the related Krein space structure and covariant field operators kab(c). We show that our gauge fixing eliminates any infrared divergence in the two-point function for the traceless part of this field. But it is not possible to do the same for the pure trace part (conformal sector). This work is in the continuation of our previous ones concerning the “minimally coupled scalar fields and the “massive” tensor field on dS.

To interpret the GRAVITY anomaly of a Koromite mine in south - west of Iran, we have used the three dimensional inversion problems. The method introduced by Last and Kubik (1983) and improved by Lewi (1997) for high precision GRAVITY data has been tested to determine the 3-dimensional form of the anomaly. The results of the inversion process have been approved by exploration drill holes in the area recently.