گسل های اصلی و خطرناک در ایران

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What are they? ‏ي‎ ‎- ۱ Faults are blocks of the earth’s crust that meet together. Scientists identify four types of faults, characterized by the position of the fault plane, the break in the rock and the MRO VEMENt af theLWA-LOGKBIOCKS.§ cain coi ‏دانشمندانآن هارا باتوجه به‎ Faults lines are under enormous pressure from the two pieces of the earth's crust pushing together. ‏ار یی از دو تطعهپوستهزمینهستند که ه هم قشار میآورند‎ خطوط كسل تحت The faults will eventually give way to the pressure causing earthquakes and creating كسل ها به زمين لرزه وليجاد مناطق كوهستائى منجر ميشوئد ‎Mountain ranges.‏ د تست 

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= = ۷ DS 0111-3 

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احلا ليلعت 

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During the last 500 years, surface ruptures associated with large earthquakes have appeared and documented in various places in lran [2, 15]. Most of these ruptures occurred along the active faults which have moved ‎ne Sane‏ ل ‎NRL RON LM IN RCN‏ زو وا ‎evidence that these active faults have the _— 

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Seismogenic ‏و‎ An underground fault which generates an earthquake but does not leave ruptures on the ground surface can be called a seismogenic fault in order to distinguish it fronvanceatthquake-fault: This types Besumiesitedd@ntitxdary Fault This type is recognized to be active based on observation of offset Quaternary landforms, however, they are not known to be seismically active. This could be due to a very long recurrence interval along ۱ One Piper trae RYE ear nn Rey smre en 

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همم CENTRAL jRAN BLOCK: 2 AFGHAN, BLOCK Tectonic setting of Iran and its subdivisions 

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The Iranian plateau is situated between the Arabian plate to the south, and the Eurasian plate to the north. As a part of the active Alpine-Himalayan orogenic belt, it is compesedof-complexsmierecontinéntal-biocks-and ocean floored basins separated by major fracture zones. ‏درایننحیهحرکت صفجهات عربی توسط ضخیمشدن پوسه رای و فورانش لیتسفری دبای عمان در زیر مکران به تحوی جبرن ده وحرکات کلی این صفحات به‎ Pe en eres In this convergent zone, the overall northward motion of the een 0 being compensated by, 1) folding and reverse faulting, resulting ina continuous thickening and shortening of the continental crust [10, 40], 2) strike slip faulting [24, 52, 67, 73], and 3) subduction of oceanic lithosphere Pane ae eee eee SU TRG ey eR ‏و‎ oe Fer ere See 

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GPS horizontal velocities show that Arabia moves at 2.1-2.5cm/yr due north relative to Eurasia [47, 67]. However, deformation is distributed differently over several active deforming zones. :درمتن ذيل نيز مقدارهاى جابه جابى ها درمناطقى لزايران كه كسل هاى شاخص را بررسى كرده ليم بر اساس مقياس سانتى متر برسال بيان كرده ايع In eastern Iran shortening is distributed over the Makran subduction complex (up to 1.9cm/yr) and the Kopeh-Dagh Mts. (about 0.6cm/yr). To the west, shortening is distributed over the Zagros (about 0.8cm/yr) [33], and Alborz Mts. (about 0.5cm/yr) [6 

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The area located between Zagros and Alborz (Central = 3 1 000 ‏قاری بلا‎ 0100700 Vari MRT «اوراسیا حرکت ی کند در ال The contrast between the velocity vectors in west-central and eastern Iran takes the form of right-lateral strike slip motion along the north-south trending ۱۱ le ecleRaRT Raut Ratan CU etch Ty diverse in different regions of Iran, an attempt is made to introduce the active Mee aM ay clean ‏و‎ ‎Be eT aol ‏حا وت ۰( ورمع !و عدءل ودف وعاوبيوطعوء ايو‎ idences 

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نقشه کسل های فعال ایران 

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۱ nut ۱ eae tee Slee ‏عط‎ ‎Caucasus to the north and the Zagros Mountains to the ‏هط خمع‌وونه عصعن۵0ط066 اه06؟ عاهنوط:۴۵ ,طانامی‎ 6 0 ‏ا ل‎ I Pe 0000 acaneeten ‏و100‎ right-lateral ریا ره یت با رت عط ع6 ی ‎ak? tec‏ انيد صطاهمع)ا ات نون ‎NW Iran of the North Anatolian fault and other right-lateral faults in SE‏ Turkey. However, right-lateral faulting in the SE Turkey-NW Iran region is not continuous but consists BoA See NTA GL ‏بات‎ age Three of these segments ruptured during earthquakes in cre 1966 

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The North Tabriz fault segment, however, has been Poe e NAL at ike Mant Rea ae ancoRe tt ecm Male PMU aoe Cn cen ura aera te i Gnome ear ate ‏ار‎ ‎1641, 1717, 1721, 1780 and 1786 earthquakes), the ‏ار ره رت وت‎ ۱۱ ‏ارام‎ ‏عوونامهه خاباه) عمهزهه مه ما م۵۵2۲ عیععر 60 ۲۵۵ وووه تزع پا ایا نیوج و‎ ۱ haem Crm Ura Ikea rR cere tM Le CCM ete OCCULT aa ‏مه ارايت عجا مز هده ره عطاش هجا نو مع وروسع 65[4] نريععا بك صل برقم ني بع عهمررنه روهو).‎ 

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000 horizontal slip rates are 1۱ ee ier nents northwestern segment of the North Tabriz fault [35]. The Khoy fault, the continuation of the Chaldiran fault, was براساس انحراف زهکشی نرخ لغزش افقی در داسه شمال غربی| قتع قارعطآر بصعاج یی 6-68۳۲ 2و 19:07 ‎ite eco mii Sec‏ براساس روادید یه سمت راست گزارش شده ات 00 ‏یر زر‎ et eR Can ‏و‎ che anrctaradcs rane Ren er enc a PE) a) eet eet aeRO uM ‏ل‎ testa aur gee cicl eT RCM RM uur esl cueuid CAPE) MK eC Lat aaa) DORE sl Re oa aes a Sena raw Ula ‏جر 9قر:0 3ه ركه وراد‎ ‏ا ا ل‎ eure marae ala 

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SOW ea cine ‏و‎ ‎Peet ‏ل‎ ‎0 ke tceeael 1 eae ۱ ‏ی‎ ele ML tcs Mal ‏ل‎ ۰ Cover Ar scel¢ 44 1s) fe i alae aa a a ‎fk unmet ag‏ دی در ‎activity has been documented using both seismicity and‏ 0 ‎The North Tehran fault, Mosha fault, North Qazvin fault, and Damghan fault (3, 5, 9, FR NESW 801005 376: ‎10, 19, 21]. Seismic activity of Torud, lpak and Abdarreh faults to the south of the ‎ ‎Alborz mountains were followed by surface faulting [1, 2, 12, 69]. The focal mechanism solution of the 1962.9.1 Buin-Zahra and 2002.06.22 Changureh Oa ‏ی‎ cll aso Le UIE Nelo mile? all 

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The Khazar fault, a reverse fault with a southward dip direction, is the longest active fault in the Alborz, and is located in the northern edge of the Alborz mountains. This Rea ee emu UN ann uMuCeA Cle auc ee y Rene ae a eR nue Cle auc TCU Eel Cretan Meee Mecca ey Ma Leilene eas 1990.6.20 was associated with 80km of discontinuous earthquake faulting [18]. The ree unmet ear) Clits oe ciara) il Mura arats CRS e ren cece cme Cena Mit ecor rl acct ۳ ‏ی ری‎ ‏نامع ععربؤعوا لوعزوو اوراص را‎ er ae ee ‏ا ا‎ peat are ee a ae و ۳ 

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In the Kopeh-Dagh, a region in northeast of Iran, strike slip MRR ‏-طعممم عط1 .ئغانه؟ معد عقون‎ ‏ممعندوع عط ما غمهمتحمملعة كغانة؟ ومتلمععع معنو رطمم‎ POSTEO ‏ال‎ emer iae len ett car ‏عون مفوه عز طءنط۷ اووه-ط۵۵۵ وا عاهتوطهه براصه عط‎ His ‏رل يا‎ 2 4 1 1 a ‎motion (right-lateral and‏ 2 ان ‎Peeters mera Pane Set ۳ ar 5‏ ‎I‏ ات الا کارت کل 00 فا ریت رن ات ی ‎erent oa 8 ie 00 27۷‏ ‎stern trends indicate a combination of left-lateral strike slip and‏ 0 ‎ee ‏بت میت ات ی و‎ RE 097۳0۵1 ۵50۳93۵۵2 ‏رش مت يو رامع ما مر سردم‎ ‎۳۳ ‎ 

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بازگشت به صفحه ‎eee‏ The focal mechanism solutions of the 1970.7.30 and 1974.3.7 earthquakes in Ree ‏ل ل لل‎ ae a cuea ice) ‏ات ری ری رت‎ rca CO CMC ieee LC Co AER lous CCR ee arate ens ‎reer ec ois y‏ ا ل یر ‎Cs TR}‏ بر را ی یر ‎۱ Renta cunt ‏ا‎ ney ۱ ‏ا‎ ‎12 ‏زر کر و‎ om cesta ‎activity of Kashafrud and Quchan faults within Kopeh-Dagh has also b 

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۱ ‏5ا0 ع مناه‎ 3 in Eastern and Central Iran ۱ ee an ‏ل‎ RCS eRe Curse ‏رت زر ور‎ Rete ره ای ‎eee eek‏ ل ‎sane Peace er cuca 00 ce]‏ 1 ‎cmicieliat‏ ا ری ی ‎era‏ ‎eee UR ace ee a a‏ ۱ ‎a teen crs‏ ۱ ما لا ‎ee eT NS PS eg Se re‏ ۹ 

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‎ae sen sate ne RUM ci Rea Mena are]‏ ا ‎eel erect em RUT Coen aio)‏ عط ماين علبروع مطعميمهم عطة 6ه طغنامد ‎Ca Cleat Nae)‏ ی یت 00 ‎predominant left-lateral strike slip movement along its east-west trend [2, 40, 70]. In‏ ا ‎Emenee ese Pa Teme ce cee nah‏ ‎BMT oti‏ ل ا ا ل 0 ا ا 00 ‎borders of the Lut region and are known to be active [13, 70]. Occurrence of the‏ ‎et ene ee‏ ا ا ا ‎Reso RSS Ed‏ ‎Cee ma uteri anes decte Ol oar Yaar ce eo‏ ۱ ‎Ce Clee Cincinnati ett‏ ال ‎Peete CCR‏ ‎ ‎ 

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۱۱ Order ae kame race eee enc nae eel ‏ومغابة؛ عع كرد ومتممعى الالال 6ه‎ ]16[. 0 ‏ا ل ل‎ ora} ا ا ی ل یزیر ‎MN NaC)‏ ی | ‎bedding plane-slip on a growing anticline [14]. Recent studies used SAR interferogam‏ ‎ec Rana‏ ل ا م ا ‎Reece Ur‏ ‎Rat ee Rte Onn Cm cc‏ 0 ‎eaceie een CT a ECO Mae ut: eran aT‏ و ‎Gee‏ ‎CCa aca EN serene‏ ره ۱ ا ‎s each‏ 000 

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کشت به صفحه اصلی .. ۱ ‏زر‎ aMi eum eae ten een cy Cretan CM AU sata enc ‏ل‎ RTS 1968:9.1 Bae eee ‏ا ا‎ راعهه موه ج۵ بط فعنوهمطمعه عهلا حعنط ۱ 6اهاوطاهه محطعامعععه 89 9:.16 :1978 ‎Nee ecICtcll‏ ی را ی سیر ۱ ‎strike slip component [11, 71].‏ Meee Cert Rien Cee ae Ceviche RT Ree ier acu rons Cm a Re eeu nea CT a Tema crs Po oe eG ens Wen de ee ee hese Sen eo eau eal ae PLT ace ‏ا ل یر ی‎ sleeve mc ves [ncaa 

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و۳ The Makran ranges are formed due to subduction of oceanic crust of the Oman Sea, with a 6km thick sedimentary cover, beneath the Asian margin [29, 75]. The eastern limit of the Makran is marked by the Chaman and Ornach-Nal faults of Pakistan. The NNW trending Zendan-Minab-Palami fault zone marks the western limit of the Makran subduction zone and connects the western Makran to the eastern Zagros deformation domain. Recent GPS studies [6] as well as geomorphic investigation [51] suggest that the Minab-Zendan- ‏یر یر یت عم 3 غ3 ومألامم ذأ ممعغؤولاد غانة؟ أممواوم‎ Ree RR ci) Makran (in Pakistan) where historical and recent earthquakes occur [25, 49], there is little ‏مماععنلطنك (صقعا مأ) مقعلقاا ممعؤدعيى عط كه ناا أمواعد لمة كغاناة؟ عباغعة عطغ مه ممغقمممكما‎ ‏اا ا ل‎ 0 UMMM ec ‏وک مر بر ناوناوه' ف هام غنم رات تسبل فقت وماد‎ ‏عت ارت نت وو ياد بابي سني ماي للك ی ی‎ 

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In view of lack of data indicating occurrence of large recent and historical earthquakes, and insufficiency of evidences in the field ‏ار‎ ‏یا‎ tec Ie eee Ue) ‎Een eS Cn Men om Tee cne eer cane ines Mae 1‏ باتوجه به كمبود داده ها نشان مى دهد ك رقر 138 اكع جرع تربع ماء تمع عطع قرط ‎IS‏ ۱ ‎S00 pea See e eT CeS‏ ان ‎SU rN hn eC‏ ‎rsh ac Seren etree‏ مجلق ام كرام كجاوا فمنط لقا ولسمة مويرم 1 كوه مم رامنا ‎Meech eek cll‏ علطن غابية؟ ماعمعمين عبتاعق مه ذأ ابرع عمع عق 1۳ ‎individual fault segments (i.e., Morvarid, Sahneh, Garun, Nahavand and Dorud [63)). T} ‏رف رت ری و یی یر ور مر رد هار ا ‎ 

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۱ emir] 1 ۱2 ‏رت‎ eee ist ae Masa Meese} ee ena ‏ل‎ ROU es Ute tec PNR U ‏ار‎ R CT Us ۱ nea eae eee ‏ل ا‎ ‏زر‎ mUIeert ee MM ‏ا‎ ie utes ‏ا رو‎ aan Pee RMS Meu Ra ‏ی‎ eto ieee ۱ ey EOD CON Reon em Cee =r Ce ate Naar eee eee a Bape athe eens eRe ed of So ‏تس ات‎ tall ‏اوسا نا‎ ۳3 ae oo ‏ا‎ 

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کشت به صفحه اصلی .. ae Ree eeu Seu Rec tele Cea enc nee ‏ا‎ to have been associated mainly with right-lateral strike-slip motion along faults that 1:۱0 ۷۰ ا ا ل ل رو ا ری ‎Cerne‏ ‏ا ری یر ل ‎ee IM eset‏ ور ۱ ‎uc ay Nees‏ ی ‎fe ey ROR‏ ‎La ela ee eae a‏ ل ‎ee eo Be atts li‏ ‎CaS acer eons See ae POM ee Nea‏ طامع معط 

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۱ Rt ee aCe ۱ er a ately ee 00 ‏یر‎ ec CS within the belt [4, 7, 8, 36, 56]. Lateral offset of Zagros fold = ot ۱ DUO EAM SCLC LUC is re 1111 ‏رت یر ای رت رس ی پر ی ار حز بر‎ cl” Run ‏كمع نادمه ععطته ممه مبمعده‎ ۱ ‏ی یر ا و‎ ری رت رو ‎areca Crees‏ ا یر ی ی زر EPSP ‏ات‎ nero N tt mete ie OM ‏ا‎ cocnerect iat 0 tea el eRe vat 

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بازگشت به صفحه اصلی . Although many of the active fault zones of Iran have been determined, many of the individual active faults are yet to be studied. Due to the geological characteristics and scarcity of accurate seismic data in Iran, it is (10 to el ny geodetic and geomorphologic methods in the اكرجه بسيارى ازمناطق كسل فعال در ايران تعبين شده استء اما بسيارى از كسل هاى فعا فردى هنوز مورد مطالعه قرار نكرفته اند . ب توجه به خصوه 3207 ee active CEU شناسی و کمبود دادههای لرزه ای دقیق در ایران؛ توصیه می شود روش های ژئودزی و ژئومورقولوژی در مطالعه رب غم ذأاغأ رمهما كه كغاناة؟ عاتاعج عط ‎Qe‏ تس ات ات ‎Tama Mel‏ .باسطح فعلى اطلاعات در مورد كسل هاى قعال ايران» امكان ايجاد رزيم كسل غالب براى كل كشوروء ‎possible to establish a dominant fat 30 3 4 =‏ 

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Strike-slip faulting in the Central and Eastern Iran. ‏اها۲0- ل نا‎ offsets across Dehshir (D), Anar (A), West Lut (WL, Se a indicated in km. ce ‎rae‏ وع2) وتمم نع عاطما م علتتواع معتقكءماءيا 5م ‎ees MN eel)‏ 0 ‎Beare a eeu eee ee‏ ‎ ‎individual faults (green numbers in mm/yr) is 

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Schematic illustration of the main ‏کااناعع۲‎ ۵۲ 6۴5 5۲0 0۴۷۵۲۵۲۰ Ll cee eed 000 Lact Sma eect a) ea SRN eteant econ uCceLactr| ‎eC Uv tra‏ ل ‎ ‎erst emer ire ai ‎GPS, geological evidence and‏ ۱ عم اقرع ]نمال ‎Fault and the associated‏ ای رای میت را پر زر ‎geformatian.zane the,velocity is deduced from the REVEL model (Sella’‏ ‎ 

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۰ ات ‎Ree eu eerie ela‏ ۱۱ ‎lines. Arrows and red uncertainty ellipses are‏ ‎eee eR CCRC UPR CCT‏ ل اك volcanoes related to collision between the Arabia and Eurasia (Kheirkhah et al. 2009). The 0 CRO Ac Perec etn Sao ve ne ‏ا‎ ECE GERM 0 ‏د‎ ا ا ا ل ان ‎RML SCS raciencam staat}‏ ا ا ‎ee ea Cpa‏ ‎all‏ ل ا لك لك ل ناویات رز رت مرت ری خلاصه نقشهپهنه بند 

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eee a ۳ 22112 ا ‎stations (light gray triangular) and IIEES‏ ‎VAUCUrl Ema Relce ec‏ 9۳۵ 02۲۲) عوهناهای ‎Fee PEER CU eyecare) Lancome‏ ‎ROPE Ut Ne Nalco Ses‏ ۱ ‎tet CONC‏ ۱ ‎selection criteria, gee the text) for local‏ ۳ ye cima anes ses ‏رهق‎ e Came ck as en gt At ear aia ane CoRR TIC CRallechitncre cence Nei ‏ذا‎ ‎ee _ ی 

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cialized study he Lake Urmia area سی تخححی کسل دریاچه ارومیه 

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۱ دمم+أ سم 0( برخی از گسل ‎ee gh‏ فعارادر ايران» از جمله گسل اصلی اخیر مطته مورد مطالعه در شمال غرب ایرانواقع شده است a) Some major active faults in Iran, including the Main Recent Fault. The study area is located in the NW of Iran. b) Shuttle Radar Topography Mission (SRTM) image from NW Iran and location of the Lake Urmia area. Fault plane solutions of recent earthquakes are presented. Active major faults around the Lake Urmia-area’are‘showf bY black lines (Main Recent Fault, North Tabriz Fault, Salmas Fault, Serow Fault, Piranshahr Fault, Urmia Fault). Extension direction marked by white arrows parallel to as aa vector measured on the exposed no; م 

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Different parts of a fissure-ridge type travertine in the Azarshahr area. a) Ridge, looking from top. b) Central part of the ridge containing vertical veins:-€} Horizontal-aragonit ‏هس‎ ical pasa coca rats 7 

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Schematic stages (left) and their equivalents in the field (right) oe 

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—— ell ‏أ7_17‎ Schematic stages (left) and their equivalents in the field (right) presenting generation and development of a travertine ridge and its central vein. a) Initiation of extensional fracture and generation of travertine ridge (for location, see Figure 2). b) Travertine ridge with recent travertine layer in white (for location, see Figure 2). c) Travertine ridge with more than 100 m height ‏سي‎ 1km i ee ee ee a: oe = 

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a) Younger horizontal travertine layers cover the steeply dipping travertine layers. Yellow arrows mark the unconformity surface. b) Paleosoil exists subparallel to the travertiné ayers. “~ 

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Rose diagrams show the strike of the measured data. Red open arrows present the exte Figure 2). نمودارهای گلسرخی 

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Traverine ridge en a) Subhorizontal layers of travertine are cut by subvertical fractures. i by younger. b) Fractures are filled by travertine breccii aragonites (marked by white arrows). ee) Ore ‏هاي باز يدون حايجابىي عمودى توليد‎ 

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a) Flat layers of pink travertine (left) are cut by the stripped vertical white travertine veins (write) containing aragonite fibers perpendicular to the fracture. Later extension gash was produced between pink and white travertine (center). Consider the long fibers perpendicular to the wall and angular patches inside the gash. 

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a) Active travertine ridge is cut and displaced by younger active normal fault; the older ridge is seen to top of the ridge (see the locations of a-c in Figure 2). b) Layered travertines were cut by younger normal faults. c) Faulted layered blocks were rotated due to further extension resulting normal faults. d) Google Earth image presents the travertine ——————— 6: 9 - 

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3D SRTM image of NW Iran. Lake Urmia area is surrounded by several major active oblique normal faults and fi is rtines: 

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Authemayou, C., Bellier, O., Chardon, D., Malekzade, Z., and Abassi, M. (2005). “Role of the Kazerun Fault System in Active Deformation of the Zagros Fold-and-Thrust ‏هدقع و لودلا لمعه‎ ¢AFEndT"V.B2RASami, K., Kozhurin, A.l., Ivanova, 1.8, Rogozhin, E.A., Hademi, M.C., and Jamali, F. (2004). “Active Faults in the Zagros and Central Baker Tectpnanysifs ‏تم‎ ‎(1993). “Earthquakes on the Kazerun Line the Zagros Mountains of Iran: Strike-Slip Faulting within a Fold-and-Thy Geophys. Journ. I erences Abdalian, S. (1963). “Le Seisme du Premier September 1962, Lihistoire Geologique et Tectonique”, Report on the Great Buyin-Zahra Earthquake of Sep. Ist 1962, Inst. Geophys., Tehran Univ., 15, 43-72. Ambraseys, N.N. and Melville, C.P. (1982). "A History of Persian Earthquakes”, Cambridge University Press, p. 219. Ashtari, M., Hatzfeld, D., Kamalian, N. (2005). “Microseismicity in the Region of Tehran”, Tectonophysics, 395, 193-208. 

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— the end we Thanks for your attention! We hope to fulfill your expectations about this project! Sj — a