IRANIAN JOURNAL OF GEOPHYSICS
Year:2017 | Volume:11 | Issue:3 |Papers Count:15

In this study, a set of models from the phase 5 of the Coupled Model Intercomparison Project (CMIP5) is used to examine the simulation of the upper-tropospheric subtropical African– Asian jet and its response to global warming. The ERA-Interim re-analysis dataset is used here to assess the model biases in representing the seasonal-mean jet features in the historical period (1980– 2005). This study analyzes the geometrical parameters of the jet including “ latitude” , “ speed” and “ width” in each season and for two separate sectors of the jet region: “ North Africa” and “ Southwest Asia” , which is briefly named “ African” and “ Asian” hereafter. The main features of the observed seasonal cycle of the jet in the re-analysis data is well captured in ensemble multimodel mean historical simulations: jet latitude increase (decrease) from cold (warm) to warm (cold) season and vice versa are correctly simulated for jet speed and width. In addition, in all seasons, the jet latitude and speed is greater in Asian sector than the African except for springtime jet speed. Despite the large inter-model spread in the historical jet simulations, the models do not show large systematic biases in most cases (seasons). However, systematic biases in each of the geometrical jet indices are found in some seasons: most models exhibit equatorward jet biases in summertime and wintertime of the African sector (about 1. 8° and 0. 9° of latitude respectively, in multimodel mean), positive biases in jet width in summertime Asia (0. 9° in multimodel mean), negative biases in jet speed in summertime Asia and wintertime of the African sector (approximately 2. 9 m/s) and positive jet speed biases in autumntime of the African sector (1. 8 m/s). There is large spread across the models in the historical jet simulations and finding the sources of this spread and the model biases is a significant challenge that should be addressed in future works. In almost all seasons and for all of the geometrical jet indices, the multimodel mean jet response to climate change is stronger in RCP8. 5 than RCP4. 5 integrations. Robustness and the quantitative value of the multimodel mean jet response in each of the jet indices vary among different seasons and sectors. In winter months, we found no robust response in any of the geometrical jet indices in African or Asian sector except for a slight and relatively robust increase in jet width (0. 2° of latitude in RCP8. 5) in African sector. However, in other seasons, we found robust multimodel mean changes in jet indices between the historical period and the end of twenty first century (2076– 2099) in the RCP8. 5 scenario: In spring, models predict a robust increase in jet width of about 0. 5° and 0. 2° of latitude in African and Asian sectors, respectively, and also a robust increase in jet speed of 1. 1 m/s for Asian sector. In summer, in the African sector, the jet speed is found to be decreased (0. 7 m/s), whereas in the Asian sector, jet speed will increase (0. 4 m/s), and it will move equatorward by 0. 8° of latitude.

Enhancement on the edges of the causative source is a tool in the interpretation of potential field data. There are many methods for recognizing the edges, most of which involve high pass filters based on derivatives of potential field data. In this paper, a new edge detection method is introduce, called the enhanced mathematical morphology (EMM) filter for interpretation of field data. The EMM filter uses the ratio of the erosion of the total horizontal derivative to the dilation of the total horizontal derivative to recognize the edges of the sources, and can display the edges of the bodies simultaneously. Edge detection of the potential eld data has been widely used as a signi cant tool for geophysical exploration technologies, which can delineate the horizontal locations of causative sources. Normally, various high-pass lters are used to recognize the edges of the potential eld data (Evjen 1936; Fedi and Florio 2001; Verduzco et al. 2004; Cooper and Cowan 2006; Cooper and Cowan 2011; Ma and Li 2012; Ma 2013). The EMM lter uses the ratio of the erosion of THD to the dilation of THD to recognize the edges of the source. Mathematical morphology was developed by Matheron and Serra in 1964 (SERRA, 1983); which is an image analysis and recognition tool. The structuring element (SE) is a basic operator in mathematical morphology, used to interact with an image and to draw conclusions about how a shape ts or misses the shapes in the image. SE consists of a matrix of 0s and 1s that can have any arbitrary shape and size. The basic operations of mathematical morphology are dilation and erosion. Dilation is de ned as the maximum value in the window ascertained by the SE. Erosion is de ned as the minimum value in the window ascertained by the SE. The EMM filter is expressed as (Lili et al., 2013): (, ) (, ) EMM Erosion F SE Dilation F SE  where imerode (F, SE) and imdilate (F, SE) represent the erosion and dilation of the THD, respectively. In this paper, a new relationship is presented for EMM filter that is tested on synthetic data with and without noise as well as the real potential field data in Qom salt dome. The EMM method successfully delineates the edges of the causative sources, which gives better resolution of the deeper source than other lters, and can display the edges of the bodies in a more centralized way. In this article, a new relationship is defined for the EMM filter as: (, ), ( ), ( ) 2 Dilation F SE Erosion F SE Dilation F SE EMM   The EMM filter was used to recognize the edges of the sources. It can display the edges of the shallow and deep bodies simultaneously. The EMM filter does not require the computation of vertical derivatives, which makes this method computationally stable. The EMM filter is tested on synthetic, and real potential field data in Qom salt dome and the edge detection was done with reasonable results.

The components of Gravity Gradient Tensor (GGT) is used for second-order derivatives of the gravitational potential field in the directions x, y and z in a Cartesian coordinate system. The third column of the gravity gradient tensor is Hilbert transform pairs of the first and the second columns. Many methods have been designed to estimate the depth, the horizontal position and the type of the sources from gravity gradient tensor components. Often, these methods are used derivatives of potential field data or their compounds in directions x, y, and z. Standard Euler deconvolution method is an approach in the interpretation of potential field data. It is able to locate the sources and to estimate the regional parameters with the assumption of the structural index. This approach is an automated method that has seen rapid development in recent years. The result of this method closely related to the precision of the assumed structural index parameter, and the accuracy is reduced in the presence of interference sources. Euler deconvolution of the directional analytic signal amplitudes is one of many methods to eliminate this problem. It is shown that the components of the gravity vector satisfy Euler's equation. Thus, it is proved that the amplitudes of directional analytic signal are homogenous and by putting in Euler's equation can estimate the location and the structural index of the gravity anomalies. In addition, two new equations were obtained from the combination of directional analytic signal amplitudes that is very effective in locating and estimating the structural index of gravity sources. This paper was examined the application of Euler's equation of the directional analytic signal amplitudes to determine the location and the structural index of gravity anomaly sources. First, it is proved that each of directional analytic signal amplitudes in directions x, y, and z satisfy Euler's equation. Second, using the combination of directional analytic signal amplitudes derived two new equations that is more successful in determining the location (horizontal positions and depth) and source type (structural index) directly over the edges of gravity anomaly sources. The maxima of analytic signal amplitude in the z-direction place directly on the edge of the anomaly sources, but the maxima of analytic signal amplitude in the x-and y-directions deviate from the edges. That is why the simultaneous use of two or three-directional analytic signal amplitude can provide more accurate solutions. The method described above was tested on the synthetic model in the presence of relatively high level Gaussian noise and interference sources. Finally, the method was applied to the Safoo manganese ore and obtained horizontal position, depth (~6 m) and structural index. MATLAB software was used to apply the abovementioned methods.

Poststack seismic inversion generally transmutes seismic amplitude to P-wave acoustic impedance, which lacks low-frequency component due to the stacking process. This component should be compensated using well logs as a priori constraint. If this low-frequency trend is known with adequate accuracy, poststack inversion could produce precise results. Nevertheless, in most cases, the mentioned information are far from the true model. In such cases, poststack inversion results could have high uncertainty. Because there is no mode conversion at normal incidence, postsatck inversion is completely acoustic, hence P-wave impedance is the only information which can be extracted from poststack inversion of P-wave data. In simulations prestack inversion, in addition to the P-wave acoustic impedance, S-wave information, density, and Poisson’ s ratio can also be derived from prestack data. Thus, prestack inversion can be used to get more information than poststack inversion. The two-step process of acoustic impedance and shear impedance by model-based inversion is replaced by one-step pre-stack simultaneous inversion. In order to apply simultaneous inversion method to our prestack seismic data, the data should be transformed from offset domain to angle domain as the first step. A useful approach is to calculate offset as a function of incidence angle, using Snell’ s Law to follow the ray path through the layers if velocity information is available. The next step is to build initial models of acoustic impedance, shear impedance, and density. We built these initial models using sonic log, Delta-Time Shear (DTSM) log and RHOB log which were available in the interest area. There are two relationships that should hold for these wet rocks. The first relationship uses this fact that in wet clastics the ratio of the s-wave velocity over p-wave velocity should be constant within a rock layer. After reformulation of the mentioned trend, one can understand that the natural logarithm of shear impedance has a linear relationship with the natural logarithm of acoustic impedance. The second fact uses Gardner equation. After reformulation of the Gardner relation, it is understandable that the natural logarithm of density has a linear relationship with the natural logarithm of acoustic impedance, too. We determined k, kc, m and mc which respectively are slope of the natural logarithm of shear impedance against natural logarithm of acoustic impedance, intercept of the natural logarithm of shear impedance against natural logarithm of acoustic impedance, slope of the natural logarithm of density against natural logarithm of acoustic impedance, intercept of the natural logarithm of shear impedance against natural logarithm of acoustic impedance. Besides, we need a set of angle-dependent wavelets which are derived from angle stacks. Hence, we built three angle stacks; near-angle stack (0 to 11 degrees), middle-angle stack (11 to 20 degrees) and far-angle stack (20 to 29 degrees). Using these angle stacks, we built three statistical angle-dependent wavelets from three angle stacks. Finally, with log information, we built an initial model for acoustic impedance and tried to solve the inversion matrix using conjugate gradient method. Solving the equation, we can derive acoustic impedance, shear impedance, and density sections simultaneously from prestack data. Using simultaneous inversion, we identified hydrocarbon reservoir.

By increasing the computing power of computers, the advantage of high-resolution numerical methods for numerical simulation of the governing equations of fluid flow is further emphasized. Recently, increasing the accuracy of numerical methods used for simulation of fluid dynamics problems, particularly the geophysical fluid dynamics problems (e. g., shallow water equations) has been the subject of many research works. The compact finite difference schemes can provide a simple way to reach the main objectives in the development of numerical algorithms, i. e., having a low cost on the one hand and a highly accurate computational method on the other hand. These methods have also been used for numerical simulation of some geophysical fluid dynamics problems. However, by splitting the derivative operator of a l compact centra method into one-sided forward and backward operators, a family of compact MacCormack-type schemes can be derived (Hixon and Turkel, 2000). While these classes of compact methods are as accurate as the original compact central methods used to derive the one-sided forward and backward operators, they need less computational work per grid point. The present work is devoted to the assessment of the accuracy of different methods. The one-dimensional advection equation with the known analytical solution is employed as a prototype model. Also, the truncation error of the traditional second-order MacCormack scheme, the standard fourth-order compact Mac-Cormack scheme, and a fourth-order compact MacCormack scheme with a four-stage Runge– Kutta time marching method are studied. Furthermore, to be able to examine the accuracy, the Lax– Wendroff, the leap-frog and the Beam– Warming methods combined with the second-order and fourth-order compact finite difference methods for spatial differencing are also used. In addition, the convergence rates of different methods are studied. It can be seen that the convergence rates are in agreement with the theoretical order of convergence. In this work, the traditional second-order MacCormack scheme (MC2), the standard fourth-order compact Mac-Cormack scheme (MC4) developed by Hixon and Turkel (2000) and a fourth-order compact MacCormack scheme with a four-stage Runge– Kutta time marching method (MCRK4) are used for numerical solution of the unsteady and non-linear Rossby adjustment problem (one-and two-dimensional cases). In the one-dimensional case, a single layer shallow water model is used to study the unsteady and nonlinear Rossby adjustment problem. The conservative form of the two-dimensional shallow water equations is used to study the unsteady and nonlinear Rossby adjustment problem in the two-dimensional case. For both cases, the time evolution of a fluid layer initially at rest with a discontinuity in height filed is considered for numerical simulations.

Dust aerosols make a considerable contribution to the climate system through their radiative effects due to their abundance in the atmosphere. Recent observations suggest that over the past decade, dust events have become more frequent in many parts of Iran, especially in the west and southwest. Through their radiative forcing, dust aerosols have significant effects on the regional radiation budget of the atmosphere, while their adverse effects on human health have also raised serious concerns. The primary aim of the present study is to examine the radiation effects associated with a severe dust storm that occurred in west and southwest Iran on 16 to 21 June 2012. To this end, the Weather Research and Forecasting with Chemistry (WRF-Chem) model was used. Two simulations were conducted: a model setup that did not include dust aerosols, and the one that included dust aerosols and their feedback to the atmosphere. A two-way interactive nested domain (nesting ratio: 1: 3) simulations were performed using 98  90 and 151  139 horizontal grid points, respectively. In the vertical, 27 σ-levels were used. The grid spacing for the two domains were 45 and 15 km, respectively. Simulations ran from 16 to 22 June 2012, and the first 24 hours was considered as the spin-up time. Meteorological initial conditions were obtained from the Global Forecast System (GFS) data at 0. 5˚  0. 5˚ resolution. The performance of the model was evaluated using the available observed data, including PM10 observations in Ahwaz located in southwest Iran, available AErosol RObotic NETwork (AERONET) data in nearby areas, and aerosol products of the Moderate Resolution Imaging Spectroradiometer (MODIS), the Ozone Monitoring Instrument (OMI) and the Cloud-Aerosol Lidar with Orthogonal Polarization (CALIOP) carried on board the Cloud-Aerosol Lidar and Infrared Pathfinder Satellite Observations (CALIPSO) spacecraft. Results indicate that PM10 concentration in Ahwaz is overestimated by the model, while simulated aerosol optical depth (AOD) is underestimated compared to the observed AERONET data. Relatively, good agreement is found between the model results and satellite products, and temporal evolution of the dust events is also well-simulated. Thus, generally, the performance of the model is acceptable for accurate simulation of the dust event. Our analysis indicated that radiative effects of dust particles cause cooling at the surface and top of the atmosphere, but warming in the middle of the troposphere. On average, perturbation of shortwave radiation by dust aerosols in the west, and southwest Iran is estimated to be-7. 27, 1. 79 and-5. 47 W m-2 at the surface, in the middle and at the top of the atmosphere, respectively. Average perturbation of the longwave radiation by dust aerosols over the same region was estimated to be 2. 2,-1. 61 and 0. 59 W m-2 at the surface, in the middle and at the top of the atmosphere, respectively. Thus, the net (shortwave + longwave) radiative effect of dust aerosols averaged in west and southwest Iran is found to be-5. 07, 0. 19 and-4. 88 W m-2 at the surface, in the middle and at the top of the atmosphere, respectively.

South of Semnan province is an important region in Iran for the formation of oil traps, which has been received much attention for several decades. Many sulfur mines have also been discovered in this area. The sulfur is most probably derived from natural gases that are guided by regional faults. Numerous anticlines and salt domes are also present in this area, playing an important role in the formation of oil traps. As a consequence, this region seems to have a great potential to form hydrocarbon traps. Since the area is covered by Tertiary, Quaternary to current sediments, gravity, and magnetic studies are very useful to investigate and explore the geological structures in this region. Gravity and magnetic studies, in a trapezium grid, were performed to investigate the underground structures, sediment thicknesses, plutonic and volcanic igneous rocks and also hydrocarbon traps. Data acquisition was carried out on 86 profiles with a northwest-southeast trend. The distance between profiles and acquisition stations were selected to be 1000 meter. Due to the presence of swamps, mountainous areas, river, terrain, etc., some stations were removed from the survey plan. In addition, some transects measured in a direction deviating from the straight line. As a result, in some of the profiles, a number of missing stations can be observed. In some of the transects, profiling was not conducted in a regular 1000 m line spacing too. The average magnetic inclination and declination are 53. 8 and 4. 2 degrees, respectively, and the average total magnetic field is estimated 48181 nT as well. The gravity and magnetic data were collected simultaneously. In this study, to interpret and discern potential field anomalies, we applied geophysical filters such as surface trend, the tilt angle, and upward continuation. After producing a geophysical map for each method, the results were jointly interpreted. Joint interpretation demonstrated that eight anticlines, five synclines, several faults and salt domes could be recognized. Among these anticlines, anticline B has a considerable depth and dimension so that with 3000 m upward continuation, the gravity field can still be seen. Meanwhile, no igneous rocks were observed on the magnetic maps. Therefore, this anticline can be considered as an appropriate trap for the accumulation of hydrocarbon. These maps confirm the joining fault to the south of Kohe-Sorkh anticline with the fault to the south of Siah-Koh anticline, which are located in the south of Abulabad. The results show that the potential methods appear to be promising to characterize subsurface structures for the initial phase of hydrocarbon explorations. These maps also show that the Siah-Kuh is a continuation of Kuh-Sorkh, which are separated by regional fault activities, erosion, and new sedimentation. Consequently, it is suggested to use numerical modeling to define the shape, dimension and depth of anomalies, especially for the interpreted anticline B. Finally, a seismic survey can be performed over the potential anomalies that might have hydrocarbon accumulation.

Natural disasters and their harmful impacts have always been one of the most challenging problems all over the world. As such phenomena are inevitable since the distant past mankind has been trying to predict them spatially and temporally and evaluate their loss. Earthquake, as a natural disaster, could not be predicted in time. However, its magnitude and location are predictable to some extent and so is the corresponding loss. Theoretical and computational advances in civil engineering lead to a precise understanding of structures’ behavior and earthquakes. Therefore, in the recent decades, nonlinear behavior and performance-based method have been introduced in the seismic evaluation of structures. Many studies have been carried out in this field by research centers and agencies like FEMA and ATC, resulted in useful guidelines. Eccentrically braced frames have high stiffness and suitable energy damping against the lateral forces like the earthquake. In this bracing system, the required stiffness and formability of the frame is provided by the link beam, and are dependent on the details and characteristics of the link beam. In recent years, Eccentrically Braced Frames (EBF) has been utilized as a resistant system against the earthquake lateral forces. The research has shown that the EBF have the ability to combine a high stiffness in the elastic range as well as an excellent ductility and energy dissipation in the inelastic range. Currently, seismic design provisions of most building codes are based on strength or force (base shear) considerations. These building codes are generally regarding the seismic effects as equivalent static forces with a height wise distribution, which is consistent with the first vibration mode shape. However, the design basis is being shifted from strength to deformation in modern performance-based design codes. Determining the shear story and overturning moment under earthquake excitation is an important problem in the seismic design of structures. There are several approaches in order to estimate an acceptable accurate response for the shear story and overturning moment of the structure in the nonlinear region. Both ATC and FEMA approaches are good ideas to evaluate the seismic performance, but more simplified approaches should be applied in seismic design codes. Most of the seismic design codes suggest a very simple relation for estimating the shear story in design base earthquake. In this study, some criterions of the mentioned guidelines are studied, which are about seismic evaluation of the eccentric braced frame (EBF) systems, then the suggestions are offered. In this research, a comparative study has been done to analyze the behavior of regular steel building structures of 4, 8, 12 and 16 stories, located in zones of high seismic hazard and soil type 2. Three-dimensional building systems composed of steel frame system with Intermediate Link Beam (EBF) have been selected for investigation. These 3D building structures have been considered with 4, 8, 12 and 16 stories. Then, the performance level of all regular structures is evaluated in one hazard level (with the return period of 475 years). In order to evaluate the performance level of the aforementioned structures, they were modeled three dimensionally using SAP V14. 00 software for both nonlinear static and dynamic analysis. The criteria for predicting the target location guidelines ATC-40, FEMA-356 and modified methods in FEMA-440 were used. The loading pattern design for nonlinear static analysis of single-mode and modal pushover (MPA) was used. For nonlinear time history dynamic analysis out of nine coupled ground motion accelerations from the strong motion database of PEER, with a minimum of 20 km and maximum 45 km from the source and magnitude range of 6 to 7. 5 were selected. The performed procedures in FEMA-356 and proposed plastic hinges in this guideline are utilized for performing the static nonlinear analysis. The soil type II was considered having the shear wave limit between 375 to 750 m/sec. The result and the accuracy of pushover analysis has been compared with the nonlinear time history analysis. This indicates that the results obtained by FEMA-440, are closer to the results of the nonlinear time history dynamic analysis. It is also concluded by the investigating of the shear story and overturning moment of the mentioned models that these parameters are dependent greatly on the length of the link beam and inadequacy of push-over analysis in demonstrating tall buildings performance are other results of this study.

Moeil Goethite iron mineralization zone related to Moeil hot streams system is located in 1 Km south of the Moeil village, at 17 km southeast of Meshkin Shahr town in Ardebil province. This zone is at the western slopes of Sabalan caldera in the northwest part of Iran. The studied area is located in Central Iran zone according to Geological Structures’ classification by Stoklin (1988) and in Alborz-Azerbayjan zone according to Nabavi (1355). General lithology of this area consists of Cenozoic and Quaternary volcanic rocks and pyroclastic material related to the Sabalan volcanism. The reason for the high thermal gradient of the region is because of hot intrusive bodies in depth. In this area, geothermal liquids move upward via fractures and fault systems when the atmospheric water is penetrated and contacted with deep intrusive bodies then hot water springs (e. g., Geinarja and Moeil) have been generated consequently. Chlorinated hot water leaches iron of Ferro-magnesium minerals, through moving beside the mafic and intermediate rocks, and deposits iron hydroxides (Goethite and Limonite) on the surface. Moeil iron ore in the south of Meshkin Shahr is considered as a prominent iron ore related to the hot water springs in Iran. In this ore, the average amount of iron oxide (Fe2O3) is 70 percent. In this paper, extension of Iron ore body, and mineralization situation was studied in depth and horizon by implementation of two geophysical approaches, including magnetic method as an indirect way for exploration of Hematite and as a method for checking possibility of magnetite mineralization in depth (about 750 data points) and electrical resistivity method as a direct measurement (seven data profiles all with lengths between 150 to 350 meters) by utilizing three different arrays at the same time (Gradient, Schlumberger and Wenner arrays) and exploration boreholes (16 boreholes with depth of 15 meters). As a result of the magnetic survey, firstly, the possibility of magnetite mineralization has been rejected. Secondly, high positive magnetic anomalies are related to granitic rocks, intermediate positive anomalies are related to Iron ore body, and low anomalies are related to springs that the minerals become precipitated. Besides, the existence of two conjugate faults with NW-SE and NE-SW directions is clear in magnetic anomaly map. In electrical resistivity pseudo sections, the presence of a nearly vertical fault is obvious. In addition, the existence of an aquifer with a very low resistivity at the bottom is detectable. Iron mineralization as a nearly horizontal layer is located between this aquifer in deep and high resistivity volcanic sediments at the top. Finally, as an outcome of this study, it can be mentioned that results of both magnetic and electrical resistivity activities, geology evidences and exploration drilling results confirm each other. In general, the below results have been achieved through Magnetic and resistivity approaches:-Magnetite mineralization is not expected in this ore due to the relatively low intensity of recorded magnetic signals.-From the magnetism viewpoint, iron layers do not have a sharp difference with base rocks (tuff).-In some points, non-ferrous volcanic rocks (granitic) show high magnetism in comparison with mineralized zones. High intensity (more than 48550 nT) is related to these granitic bodies.-The intensity between 48550 nT and 48800 nT is related to the iron mineralized zone.-Results from geoelectric studies show that the specific resistivity between 150 and 700 ohm-meter is related to the iron layers, and the figures between 700 and 800 ohm-meter is associated with pyroclastic materials and volcanic rocks.

From ancient times, celestial bodies have been used by travelers and scientists for positioning and routing. By developing sciences, it was found that the celestial bodies form an accurate inertial system to use in navigation applications. In this system, each star is considered as a reference point in determining reference coordinate frame of the system. Due to the visibility of the satellite motion trace and the fundamental need to determine and modify satellites’ orbital parameters as well as to identify and locate espial satellites, determining the positional parameters of the satellite is also one of the modern and important applications of vision-based astronomical systems. In the modern vision-based astronomical systems, data collection is done using charge-coupled device (CCD) array. During the process of light collision to the surface of the CCD and then reading and measuring the number of photoelectrons as well as converting them to the digital numbers to store them as grey degree in each pixel, the smallest mistakes that result in lost or added electrons on each pixel can lead to distortion and noise in the image. The process of noise elimination should not only eliminate or reduce the noise but also avoid blurring the image and removing or relocating the edges of the image. To determine the primary orbit of the satellite using an optical method, the streak of the satellite must be extracted accurately because the misdiagnosis of the beginning and end points of the streak directly affects the accuracy of the determined orbit. Therefore, we need to find noise elimination methods that impose the lowest possible effects to the key complications of the astronomical images such as star and satellite streak. In this study, it is attempted to eliminate the noises using diffusion equation and solving it numerically. On the other hand, to identify the accurate position of the edges, the gradient is calculated by through convoluting the main image by the Gaussian filter. In this study, a numerical method is used to solve diffusion equation. Heat diffusion equation is an iteration-based method. It is obvious that the more the paces and iterations in the equation, the smoother the image. This factor must be chosen such that the image brightness does not exceed the main range. For this purpose, the noise must be eliminated from the image by choosing appropriate number of iterations. In this research, the structural similarity index (SSI) is used to select the optimum number of iterations. As a result, in this research, it is attempted to use noise elimination methods that impose the lowest changes to the existing satellite’ s streak.

Ground-penetrating radar (GPR) is a popular geophysical method for high-resolution imaging of the shallow subsurface structures. Numerical modeling of radar waves plays a significant role in interpretation, processing, and imaging of GPR data. A number of different approaches have been presented for the numerical modeling of GPR data. The most common approach for GPR modeling is the finite-difference method (FDM) because the FDM approach is conceptually simple and easy to program. The difficulties in applying boundary conditions at non-linear boundaries and the lack of sufficient accuracy in complex geometries are the most important drawbacks of FDM. This paper presents a finite-element method, for simulation of ground-penetrating radar (GPR) in two dimensions in the time-domain. FEM is a powerful and versatile numerical technique for handling problems involving complex geometries and inhomogeneous media. The technique is based on a weak formulation of Maxwell’ s equations. In the FEM method, the wavefield is discretized on the elements using Lagrange interpolation, and integration over an element is accomplished based upon the Gaussian-quad integration rule. The major difference between the various numerical methods is in the spatial discretization. In the elementalbased methods, the complex geometry of the problem is divided into several smaller and simpler elements, then the integrals are calculated for each element. These methods have no with any regular or irregular geometry. The responses of the model in the finite-element methods are approximated in nodal points, so nodal polynomials of Lagrange are used for interpolation of the model response. Besides, the systematic generality of the method makes it possible to construct general-purpose computer programs for solving a wide range of problems. In this paper, at first, Maxwell’ s equations are discretized, then the boundary condition is applied to minimize artificial reflections from the edges of the computation domain. Although the governing equations and mechanisms are completely different between radar and seismic waves, most of GPR data processing approaches are derived from seismic data processing. Due to similarities in these two techniques, accordingly, we implement the first-order Clayton and Engquist absorbing boundary conditions (first order CE-ABC) introduced in the numerical finitedifference modeling of seismic wave propagation. This boundary condition is simple to apply. The presented formulations are in matrix notation that simplifies the implementation of the relations in computer programs, especially in MATLAB application. After spatial discretization with FEM, time discretization is done by Finite-Central Difference (FCD). The time discretization is the most massive and time-consuming step in modeling, which spatial discretization has an important role in this process. The stiffness, mass and damping matrices are sparse and symmetrical in FEM; so if we use the optimized numerical algorithms and storages strategies, computational costs and processing-time can be reduced significantly. To investigate the efficiency of FEM, the computer program has been written in MATLAB and has been tested on two models. The results show that the radar wave simulation via FEM is an accurate and effective approach in complex models.

We analyzed the teleseismic data gathered by a broad-band (CHBR) and four short-period (CDK, CNT, KHB, KSM) seismometers, located in western coastal Makran, north of Chabahar, Iran. The data were gathered by the roughly north-south direction quasi-linear profile and used to calculate P (for all stations) and S (only for CHBR) receiver functions utilizing iterative deconvolution technique of Ligorria and Ammon (1999). Because of backazimuth gaps in south and western directions, we used PKiKP and Pdiff phases to calculate receiver functions in a similar processing approach. Calculated P receiver functions are migrated to depth to clarify the geometry of velocity boundaries at the base of sediments and Moho. The result shows that there is a dipping interface lying at a depth of 27 km (beneath CHBR) to 31 km (beneath CDK), which imply a 2. 5o dipping Moho boundary beneath the study region. To avoid the trade-off between velocity model and reported depth, we jointly modeled the stacked receiver function, and group velocity dispersion curve for CHBR and the output model was considered for any time to depth migration of receiver functions. We analyzed the effects of P and S anisotropy on teleseismic converted waves to map the presence, the strike, and the depth of anisotropic structures. High-resolution PRFs are considered for such analysis. The following criteria are considered to select the high-quality receiver function (Schulte-Pelkum and Mahan, 2014): the signalto-noise ratio of the three components of the seismograms is at least 1. 5; the convolution of the PRF with the vertical component of the seismogram reproduces at least 60% of the horizontal component (defined as variance reduction by Ligorria and Ammon, 1999); the PRF shows a positive polarity direct P arrival; the receiver function amplitude does not exceed 1; any arrivals’ pulse length does not exceed 3. 5 s. The latter two criteria are employed because very high amplitudes and long oscillatory pulses are typical characteristics of an unstable deconvolution (Schulte-Pelkum and Mahan, 2014). The calculated PRFs were then binned in 5° azimuthal groups with 5° overlap. In CHBR station, we recognized signs of the top (at 1 km depth) and bottom (at 9 km depth) of an anisotropic layer with almost north-south anisotropic symmetry axis. In addition, we recognized a flat interface beneath CHBR station at 27 km depth that is not in consistency with the result of migration to a depth of RFs showing a 2. 5o dip Moho at the same place. For this reason, we utilize forward modelling to calculate synthetic PRFs to explain periodic amplitude variation of P to S converted phases with back-azimuths in each station that could be a signature for anisotropic velocity features. The forward modeling indicates that the horizontal interface makes a similar pattern on simulated PRfs as a low angle dipping interface with dip less than 10o. Migration of S receiver functions reveals a deep velocity discontinuity at depth around 80 to 100 km that might be considered as a shallow lithosphere-asthenosphere boundary beneath the study region.