Determination of velocity of seismic waves and upper crustal velocity model in Shiraz seismological network

Iran is located between two lithospheric plates (Euroasia, Arabian) and these two plates converge toward each other with a velocity of 25 mm/yr rate. Shortening that produced from this convergence with Makran subductin shows faulting and folding in Zagros orogenic belt, Alborz and Kopedagh in north and sliding in sum strike slip faults with north-south trend in central Iran.
The NW-SE trending Zagros fold and thrust belt, extends for about 1800 km from a southeast of the East Anatolian Fault in northeastern of Turkey to the Strait of Hormuz, where the north-south trending Zendan-Minab-Palami fault system separates the Zagros belt from the Makran accretionary prism.
The Zagros range currently accommodates almost half of NS shortening between the Arabia and Eurasia. This active fold and thrust belt is subdivided into five morphotectonic units: the High Zagros Thrust Belt, the simple Fold Belt, the Zagros Fordeep, the Zagros Coastal Plain and the Persian Gulf-Mesopotamian lowland. The studied region in this paper located in Fars province, in the High Zagros Thrust Belt, north Eastern part of this region is Abarkuh desert that located in central Iran is less active than the other border region around studied region.
The west and southeastern part of this region is located in Zagros seismotectonic province that a lot of earthquakes were seen. For study of velocity of seismic waves and upper crustal velocity model in Shiraz region the recorded data by Shiraz seismic network during 2002 to 2009 were used and for seismicity, International Seismological Centre (ISC) catalog, Harvard Centroid Moment Tensor (CMT) catalog and historical earthquakes catalog (Ambraseys and Melville, 1982) were used.
Crustal structure of this region is a particular issue that is not yet resolved in the studied region. In order to study the crustal structure of studied region, we use Shiraz network that have 5 stations, To assesse the velocity model, subset of 78 events was selected that recorded by minimum of 4 stations, with an azimuthal gap less than 270?, residual RMS less than 0.3s and uncertainties in epicenter less than 6 km and depth less than 10 km. Consequently using these events, a crustal velocity model obtained with VELEST software for the upper crustal velocity model beneath studied region.
The calculated velocity model for the studied region showed three discontinuities in 6, 10 and 14 kilometer depths. P wave velocity has been obtained 5.68 km/s, 5.88 km/s, 6.54 km/s and 6/66 for the first layer, second layer third layer and half space, respectively.
Plotting Tsj-Tsi (S arrival time to stations i and j respectively for same event) versus Tpj-Tpi (P arrival time to stations I and j respectively for same event) for all events and all stations, Vp /Vs ratio was computed about 1.77 with 908 arrival times.
Comparison of obtained VP/VS value with other research results shows that there is not a significant difference between them. Also, local velocity curves for Pg, Pn, Sg, and Sn phases are obtained in the study area by using the data base 2002 through 2009. The slopes of these curves give crustal P and S velocities of 6.16±0.02 and 3.71±0.02 kms-1, and Moho P and S velocities of 7.8±0.1 and 4.78±0.04 kms-1, respectively.