NORTH OF TEHRAN SITE EFFECT MICROZONATION
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1 13 th World Conference on Earthquake Engineering Vancouver, B.C., Canada August 1-6, 2004 Paper No NORTH OF TEHRAN SITE EFFECT MICROZONATION M.K. Jafari 1, M.Kamalian 2, A.Razmkhah 3, A.Sohrabi 4 SUMMARY Tehran is located in one of the most earthquake-damaged zones in Iran. Earthquakes have repeatedly struck Tehran region during the previous centuries. The site effect microzonation project of north Tehran started in The available geotechnical data in this area was gathered. Comprehensive refraction geoseismic investigations as well as microtremor studies in north of Tehran have been performed. Based on the above-mentioned data and investigation results, the microzonation maps including natural site period map, dynamic site period map, PGA distribution map and PGV distribution map have been provided. Furthermore, the effect of topography in north of Tehran on microzonation results will be studied and considered. INTRODUCTION In 1993 IIEES initiated a comprehensive seismotectonic, seismic hazard, geotechnical hazard, vulnerability and risk studies for Tehran. The geotechnical microzonation part of the program was composed of two parts: site effect and liquefaction potential microzonation. Site effect microzonation started for south of Tehran by using analytical as well as microtremor measurements studies which has resulted to the presentation of the three microzonation maps (natural site period map, dynamic site period map and the PGA distribution map) for south of Tehran. To increase the accuracy of the performed microzonation project, two projects has been planned and performed: complementary studies on the south of Tehran for updating the existing microzonation maps with a comprehensive field and laboratory (static and dynamic testing of the collected samples) testing program and site effect study of northern part of Tehran.. The site effect microzonation project for north of Tehran started in In this area, the topographic effect should also be taken in to consideration, Figure (1). The available geotechnical data in this area was 1-Associate Professor, Director of Geotechnical Eng. Research Center of IIEES, I.R. Iran, Jafari@iiees.ac.ir 2- Assistant Professor, Geotechnical Eng. Research Center of IIEES, I.R. Iran, kamalian@iiees.ac.ir 3- Assistant Professor, Islamic Azad University, South of Tehran Campus & IIEES, I.R. Iran, ar.razm@iiees.ac.ir 4- Ph.D. Student, IIEES, I.R.Iran, sohrabi@iiees.ac.ir
2 gathered (more than 400 borings) and the refraction geoseismic investigations (38 locations) as well as microtremor measurements (55 stations) in north of Tehran have been performed. Based on the above-mentioned data and investigation results the microzonation maps including natural site period map, dynamic site period map, PGA distribution map and PGV distribution map have been provided. Also and based on detailed parametric studies (Kamalian, [1] & Razmkhah [2]), the 2D effect of local topographic features on natural site period and amplification factor have been evaluated. In this paper, the summary of the results will be presented and discussed. SURFACE GEOLOGY, SEISMOTECTONIC AND SEISMIC HAZARD Surface Geology The North of Tehran area forms mainly from Tehran alluvium, which can be divided to four formations: A Formation (HezarDareh) - it consists of homogenous gray and cemented conglomerates in the thickness of 1200 m. The formation has a high internal fraction degree and so, can be stable in the over steepened slope. The lower parts of the formation indicated by low permeability, weathered and high strength layers. In the upper parts, the permeability and the weathering increase and the strength decrease. B Formation (Kahrizak) it forms from unconsolidated and unsaturated conglomerates, which consists of gravel, sand, silt, clay and randomly the big slabs of the rock. The formation discordantly overlaid on Hezardareh formation and can be distinguished by its darker color and gentler slope (Max. 15 degree). Its color, due to clay, is dark red. The thickness of the formation is variable and in the thickest parts, can reach to 60 m. C Formation (Tehran plain alluvium) - it forms from gravels, pebbles and sands in the cement of sands and silts. The permeability and the strength of the formation are high. The volume of Tehran alluvium fans consists mainly of C formation. As to more thickness and permeability, it forms a suitable groundwater resource in Tehran. D Formation (Recent alluvium) - the most recent riverbeds, alluvium terraces and the young fans consist of the D formation. It includes gravel and pebble, by the weak cements in the north, which gradually convert to silt and clay toward the south. Due to weathering, a layer with the thickness of 2-3 m is formed on the surface of the formation Seismotectonic The city of Tehran is located in the front of the Alborz Mountain which is a tectonically active region situated between the Caspian Sea and the Iran platform. The tectonic of Alborz mountain belt is controlled by the boundary condition due to the convergent motion between Arabia and Eurasia, which probably started in the Cretaceous. The folding is accompanied by the fast subsidence of the South Caspian Sea where several kilometers of sediment have been accumulated. Also there is an abrupt change of about 2750m in elevation between the city and the nearest summit of the northern mountain range, which is a striking topographic feature. Several major faults run parallel to the Alborz fold-thrust mountain belt at its foothill near the Tehran. The most active faults are the Musha fault, which is 400km long dipping northward and changing direction to EW. North Tehran fault striking EW at the immediate foot of the Alborz with more than 75km is smaller in dimension and might be due to the vertical movement along the major mountain bordering. Besides, smaller faults such as North Rey, Garmsar, Kahrizak, Parchin and Ipak faults and many minor faults are widespread throughout the city and reactivation of major quaternary faults may cause some movement along the minor faults.
3 For better assessment of the fault activity, active faults are therefore observed around Tehran. However, the kinematics of the different faults is not precisely known and the relation with seismicity in not clear. Thus a comprehensive seismotectonic study of Tehran including fault-stress analysis, trenching, paleoseismology, satellite geodesy, InSar imagery, absolute gravity measurements are underway at IIEES Seismicity and Seismic Hazard Historical earthquakes are reported in the area of Tehran around the Musha, North-Tehran, North-Rey faults, etc. Because of the sparse population and cities, it is difficult to have a complete record of the past strong earthquakes. Despite the limited available seismic data, a short review of the historical earthquakes in Tehran indicates that the region is highly seismic and has experienced several destructive earthquakes.the occurrence of more than 10 earthquakes with magnitude around 5 during the 20 th century in the Tehran region indicates activitiness of the faults. Based on separated research project (Zare, M. et al., [3]), seismic hazard analysis of study area for 475 years return period showed that the peak rock acceleration in north of Tehran could be assumed about 0.41g. If the epicentral distance in the study area was considered less than 50 km, then according to attenuation curves (Seed, H.B. et al., [4]), the predominant period of the rock motion could be assumed about 0.3 seconds. Geotechnical Profiles BASIC DATA Soil profiles were determined from compiling the data of about 400 existing borings at more than 100 locations and available geological and geoseismical data, Figure (2). The subsurface soil layers were classified as cohesive and granular and each class was further classified according to its stiffness or density respectively. Since boring data were not available in all the units of our mesh, the units were grouped into a number of representative soil profiles according to generic ground conditions. V s SPT Correlation Geoseismic investigations and in- situ measurements of shear wave velocity were made at 38 locations by refraction method, Figure (3). Among the various existing Vs SPT correlations in the literature (Jafari, M.K., Shafiee, A., Razmkhah, A., [5]) and based on previous microzonation studies (Jafari, M.K. and Asghari, E., [6] & Jafari, M.K., Pourazin, Kh. and Kamalian, M., [7]) as well as gathered geotechnical and geophysical data, the one proposed for the Balkan region was selected and slightly modified. The used correlation is summarized in Table (1). Table (1): Classification of Tehran s soils based on shear wave velocity Cohesive Soils Granular Soils Soil Class C1 C2 C3 C4 C5 N1 N2 N3 N4 SPT < >50 < >50 Vs (m/s)
4 Input Motion Since there are no strong motion time histories for Tehran earthquakes, 13 time histories were selected from the existing data bank of recorded earthquakes around the world with similar distance and hypocentral conditions and frequency content expected in Tehran. Then, selected time histories were normalized for a PGA of 0.41g and a predominant period of 0.3 seconds. SITE RESPONSE ANALYSIS 1D Site Response Analysis and Microzonation Maps In this study, the basic site response effect was evaluated using the SHAKE computer program (Schnabel, P.B. et al.,[8]). The ground surface conditions in north of Tehran was assumed 1D, which are suited for SHAKE analysis and in the next step the effect of topography on the 1D results has been studied. Each representative soil profiles were analyzed using the previously mentioned normalized time histories. Based on the calculation results and microtremor measurements, microzonation maps consisting distribution of natural site periods, Figure (4), dynamic site periods, Figure (5), PGA, Figure (6) and PGV, Figure (7) throughout the study area were prepared. 2D Effect of Topography The evaluation of microzonation studies with similar topography conditions to north of Tehran could be done using one of the following approaches: Neglecting the surface or subsurface topography and performing 1D analysis, Performing site response analysis of representative 2D profiles (N-S or E-W) in the studied area and modifying 1D results. On the other hand, it seems that the difference between general and local topography should be considered. General topography is attributed to large scale irregularities such as north-south general slope of Tehran, meanwhile local topography is related to small scale irregularities such as local ridges or hills. Preliminary studies (Dehghani, A. and Jafari, M.K., [9]) on the 2D site response analysis of a northernsouthern profile of Tehran and corresponding 1D analysis showed that with microzonation investigation objectives studies and expected accuracy, general topography of Tehran does not have any considerable effect on the results of site response analysis. Nevertheless, for evaluation of the effect of local topography, wide range 2D parametric studies through various geometrical and geomechanical parameters of different shapes of ridges have been performed and the effect of such irregularities on the 1D microzonation procedure has been determined and a simple method has been proposed for considering 2D effects based on 1D results (Kamalian,[1] & Razmkhah[2]). These results showed that, at north of Tehran and with regard to small values of shape ratio of the existing local topography in this area, the amplification factor hasn t been exceeded more than 15 % with respect to 1D results but the natural site period in 2D case have been varied considerably, Figs (8) & (9) (Razmkhah[2]). MICROTREMOR MEASUREMENTS It is over three decades since microtremors are being used to investigate the amplification characteristics of soils. In parallel with geoseismic investigations, the microtremor measurement was also performed in 55 stations in the north of Tehran, Figure (10). Two objectives were fixed for these measurements: First, comparing the measured and calculated (from 1D SHAKE site response analysis) natural site period and second, controlling the selected seismic bedrock where the sufficient geotechnical parameters were not available. In many of the measured points there were a good correlation between the value of the natural
5 periods obtained from microtremor measurements and site response analysis (Razmkhah, A., Jafari, M.K. and Ghayamghmian, M.R., [10]). The most part of the non-conformity of results corresponds to the region where the subsurface layering is rather complex and not correctly evaluated. CONCLUSION North of Tehran site effect microzonation study was performed based on 1D site response analysis. The microzonation maps including natural site period, dynamic site period, distribution of PGA and distribution of PGV have been provided. In addition 1D results, also 2D natural site period maps has been presented. Also, obtained results showed that, with consideration the general and local topography of Tehran s North, considerable amplification was not occurred and with regard to small values of shape ratio of the existing local topography in this area, the amplification factor hasn t been exceeded more than 15 % with respect to 1D results. The one-dimensional PGA distribution map showed that in most of study area, the effect of presence of alluvium layer on the input motion, due to insignificant thickness and considerable compaction of this layer, had a little effect. AKNOWLEDGMENTS This research project has been supported by Grant No. NRCI 5018 of National Research Projects and supported by National Research Council of Islamic Republic of Iran. REFERENCES 1. Kamalian, M., (2004) The effect of topographic features on seismic response of ground surface, ongoing research project, IIEES, Tehran, Iran 2. Razmkhah, A., (2004). Evaluation of the effect of topographic features on ground surface seismic response: Tehran case study, Ph.D. Thesis, Islamic Azad University, Science and Research Campus, Tehran, Iran(In Persian). 3. Zare,M. et al., (2003). Seismic Hazard Analysis of Tehran, ongoing research project, IIEES, Tehran, Iran. 4. Seed, H.B., Idriss, I.M. and Kiefer, F.W., (1969). Characteristics of rock motion during earthquakes, Journal of the Soil Mechanics and Foundation, Division, ASCE, Vol. 103, No.GT6, USA. 5. Jafari, M.K., Shafiee, A. and Razmkhah, A., (2002). Dynamic Properties of Fine Grained Soils In South of Tehran, Journal of Seismology and Earthquake Engineering, Vol. 4, No. 1, Tehran, Iran. 6. Jafari, M.K., and Asghari, E., (1998). Seismic Geotechnical Microzonation of Southwest of Tehran, IIEES Report No , Tehran, Iran ( In Persian ). 7. Jafari, M.K., Pourazin, Kh. and Kamalian, M., (1999). Seismic Geotechnical Microzonation of Southeast of Tehran, IIEES Report No , Tehran, Iran ( In Persian ). 8. Schnabel, P.B., Lysmer, J. and Seed, H.B., (1991). SHAKE, A Computer Program For Earthquake Response Analysis of Horizontally Layered Sites, Earthquake Engineering and Research Center, Berkeley, California, USA.
6 9. Dehghani, A. and Jafari, M.K., (1996). Effect of Topography on the Site Response Analysis, M.Sc. Thesis, Sharif University, Faculty of Civil Engineering, Tehran, Iran( In Persian ). 10. Razmkhah, A., Jafari, M.K. and Ghayamghamian, M.R., (2002). Microtremor Measurements in North of Tehran, Proceeding of 3 th International Conference on Geotechnical Engineering and Soil Mechanics (ICGESM3), Tehran, Iran( In Persian ). Figure (1) Study Area Figure (2) Distribution of Collected Geotechnical Data
7 Figure (3) Distribution of Geoseismic Profiles Figure (4) Distribution of Natural Site Period Figure (5) Distribution of Dynamic Site Period
8 Figure (6) Distribution of PGA Figure (7) Distribution of PGV
9 Figure (8) Distribution of 2D Natural Site Period(N-S) Figure (9) Distribution of 2D Natural Site Period(E-W) Figure (10) Microtremor Measurements
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