Determination of causative fault parameters for some recent Iranian ...

Journal of Asian Earth Sciences 25 (2005) 621–628
www.elsevier.com/locate/jaes
Determination of causative fault parameters for some recent Iranian
earthquakes using near field SH-wave data
H. Hamzehloo*
International Institute of Earthquake Engineering and Seismology, Farmanieh, Dibaji, Code 1953714453,Tehran, I.R. Iran
Received 8 December 2003; accepted 29 June 2004
Abstract
A method based on a point source representation and non-linear least square formulation, which estimates the strike, dip and rake of the
causative fault, has been used to infer the causative fault plane parameters using strong ground motion data for the some recent earthquakes in
Iran. This study indicates that the analysis of SH-Waves of near field accelerographs can distinguish the fault plane from the auxiliary plane.
This method is especially helpful, when lack of information such as surface rupture, aftershock data and isoseismal maps makes it difficult to
identify causative fault plane in the fault plane solution. The estimated fault plane parameters from inversion of the near field data based on
the point source model for these earthquakes are in fair agreement with solutions given by HRV and NEIC.
q 2004 Published by Elsevier Ltd.
Keywords: Causative fault; Near field; SH-waves; Point source; Non-linear least square
1. Introduction
The Alpide–Himalayan seismic belt is recognized as one
of the most seismically active areas of the world. In Iran this
belt is defined by a broad band of diffused seismicity and
contains several mobile belts surrounding small, relatively
stable blocks. The seismicity of Iran has been discussed by
several authors (Gutenberg and Richter, 1954; Niazi and
Basford, 1968; Nowroozi, 1971, 1976; Berberian, 1976;
Shoja-Taheri and Niazi, 1981). The major zones of
mobility, in decreasing order of activity, are Zagros, Alborz,
East-Central Iran and the Caucasus and Eastern Turkey,
although some small aseismic blocks in central Iran, in the
northwest of Iran and the south Caspian Sea exhibiting
noticeable stability have also been identified.
The Zagros Fold Belt extends from south-eastern Turkey,
through the whole of southern Iran to a north-trending
transcurrent fault near the Strait of Hormoz at the mouth of
Persian Gulf. The fold belt is a result of the collision of the
Arabian Plate from the southwest with central Iran in
the northeast. Earthquakes have occurred throughout
* Tel.: C98-21-2831116; fax: C98-21-2299479.
E-mail address: hhamzehloo@iiees.ac.ir.
the 200–300 km width of the Zagros Mountains (Fig. 1).
Various investigators have studied the depths of the larger
Zagros earthquakes using teleseismic P-waveforms (e.g.
Jackson and Fitch, 1981; Kadinsky-Cade and Barazangi,
1982; Ni and Barazangi, 1986). Hypocenters are mostly in
the depth range of 8–15 km. Study of the historical
seismicity (pre-1900) of the Zagros active folded belt
shows that this region has been devastated a number of
times (Berberian, 1976). Baker et al. (1993) mentions that
most of the larger (m b R5.0) earthquakes in the Zagros have
occurred along the southwest front. Most large earthquakes
have fault plane solutions that show high-angle (30–608)
reverse faulting on a plane parallel to the local strike of the
belt (McKenzie, 1972; Jackson and Mckenzie, 1984). The
Kazeron fault reported by Baker et al. (1993) shows strikeslip
movement within a fold and thrust belt. Berberian
(1976) mentions that some basement trends are present in
the Zagros, which are roughly aligned, in a north–south
direction and the focal mechanism of these earthquakes
would be strike-slip/or normal faulting. According to Baker
et al. (1993) such basement faults are unlikely to propagate
to the surface through several thick horizons within the
sedimentary cover. This is usually taken as the explanation
for the remarkable lack of surface faulting following Zagros
1367-9120/$ - see front matter q 2004 Published by Elsevier Ltd.
doi:10.1016/j.jseaes.2004.06.005

622
H. Hamzehloo / Journal of Asian Earth Sciences 25 (2005) 621–628
Fig. 1. The HRV located epicenters for the 1994 Zanjiran, the 1997 Ardebil, the 1999 Kareh Bas, the 2002 Avaj, and the 2003 Jahrom earthquakes are shown
with Stars. NTF: North Tabriz Fault; KF: Kazeron Fault.
earthquakes of large magnitude (Berberian, 1976; Berberian
and Papastamatiou, 1978; Jackson and Fitch, 1981;
Ambraseys and Melville, 1982,). According to McKenzie
(1972) interpretation of fault plane solutions in Zagros is
hindered by the absence of observed surface ruptures.
The pattern of seicmicity in the Alborz is discontinuous,
with gaps filled in gradually by relatively large events. Most
of the strong earthquakes are in the eastern and central
Alborz regions. Considering macroseismic data, Ambraseys
and Melville (1982) have found that the large scale
seismicity of the region does not follow any pattern
apparent from surface tectonics, nor is it dependent on the
major known Quaternary faults in the area. Recent large
earthquakes occurring in this region suggest that the
seicmicity is connected with relatively major faults of
recent age that cut across the regional Quaternary
lineaments.
According to Berberian (1979), central Iran is not a linear
seismic zone. It is characterized by scattered seismic
activity with large magnitude earthquakes, long recurrence
periods and seismic gaps along several Quaternary faults
(Fig. 1). The shocks in central Iran are generally shallow and
are usually associated with surface faulting. The Azarbaijan
province in northwest Iran is bounded in the southwest by
the north Tabriz Fault that has a northwest–southeast trend
(Fig. 1). The northeast boundary is a major fault that
separates this province from the Caspian shore province.
The seismicity in this province is sporadic and does not
show well-defined trends (Nowroozi, 1976). According to
Ambraseys and Melville (1982), lack of earthquake
information for the Ardebil area suggests that no earthquakes
of any significance have affected this area in the
recent past. A study of historical earthquakes (pre-1900)
shows that only a few earthquakes have occurred in this
region.
2. Method
A fault plane solution yields information about the nature
of an earthquake. In addition, the usefulness of focal
mechanism studies must be emphasized in its application to
research on regional and global tectonics (Kasahara, 1981).
A fault plane solution allows us to determine the mode of
stress change in the earth, at the specific time and locality of
an earthquake. The information yielded by focal mechanism
studies gives an instantaneous picture of tectonic movements.
Several methods are available to estimate focal
parameters such as first P-motion, S-waves, spectral
amplitude of body wave, finite moving source, surface
waves and moment tensor solution.
Strong motion data play an important role in studying the
nature of an earthquake. Strong motion recording close to

H. Hamzehloo / Journal of Asian Earth Sciences 25 (2005) 621–628 623
Table 1
Source parameters of selected earthquakes
Earthquake Location of earthquake hypocenter M W NP1 NP2
yy/mm/dd
8N 8E km Str Dip Rake Str Dip Rake
1994/6/20 29.06 52.44 15.0 5.9 251 67 K5 343 85 K157
1997/2/28 38.30 48.06 15.0 6.1 184 57 K15 283 77 K146
1999/5/06 29.34 52.03 17.4 6.2 52 76 K6 143 84 K165
2002/6/22 35.85 48.94 16.8 6.5 304 26 110 102 66 80
2003/7/10 28.41 54.02 15.0 5.6 305 42 118 91 49 66
earthquake source gives more confidence in the estimation
of the causative fault. The Iranian Strong ground motion
network, which has been installed by the Building and
Housing Research Center (BHRC), includes more than 1000
strong ground motion stations in Iran. The availability of
strong ground motion data from Iranian earthquakes helps
us to study earthquakes in more detail. The aim of this study
is to infer the causative fault plane parameters using strong
ground motion data, and show how these data can help us to
identify the fault plane in the focal mechanism solution,
especially when lack of information such as surface rupture,
aftershocks data, and an isoseismal map make it difficult to
identify the fault plane in focal mechanisms reported by far
field data. Recently, Sarkar et al. (2003) have analyzed the
strong ground motion of the 1990 Rudbar earthquake to
infer the characteristics of the source. SH-wave (horizontal
shear wave) analyses of accelerograms exhibit distinct
phases corresponding to energy released from three separate
asperities on the discontinuous segments. The strike, dip,
and rake for the three subevents have been estimated (Sarkar
et al., 2003). The method of Sarkar et al. (2003) has been
used to estimate the causative fault parameters. This method
is based on a point source representation and non-linear
least square formulation which estimates the strike, dip and
slip of the causative fault and a grid search technique that
provides separate estimates of the strike, dip and slip. The
analysis is confined to SH-waves because these are
minimally affected by crustal heterogeneity (Haskell,
1960). Corresponding theoretical estimates of SH-wave
amplitudes of displacement are obtained from the formulae
for the radiation pattern of SH-waves in a full space (Aki
and Richards, 1980; Lay and Wallace, 1995). The error
function E (strike, dip, rake) is represented as:
Eðstrike; dip; rakeÞ Z X i
ðA oi KA ti Þ 2
Here A oi and A ti denote the observed and theoretical
amplitudes of the near field SH-wave displacement at the
selected frequency at the ith station. The summation is over
all stations that recorded the particular event. The non-linear
Newton technique is used to obtain those values of strike,
dip and rake which optimize E (strike, dip, rake) in the least
square sense.
To estimate causative fault plane parameters, near field
strong ground motion data have been analysed for the 1994
Zanjiran earthquake, the 1997 Ardebil earthquake, the 1999
Kareh Bas earthquake, the 2002 Avaj earthquake and the
2003 Jahrom earthquake. Location of these earthquake and
their parameters are shown in Fig. 1 and Table 1.
3. Data
For this study, high quality reliable data, which show
signal to noise ratio greater than 3, have been considered.
Only data pertaining to the SH wave, are used. For
appropriate selection of SH-wave components of the
recorded data the radial (L) and transverse (T) components
of recorded acceleration and displacement are suitably
rotated so that corresponding estimates along and perpendicular
to azimuth direction are obtained. The rotated
transverse components provide acceleration and displacement
data of SH-waves, recorded at each of station. The SHwave
acelerogram records for the 1994 Zanjiran earthquke,
the 1997 Ardebil earthquake, the 1999 Kareh Bas earthquake,
the 2002 Avaj earthquake and the 2003 Jahrom
earthquake are shown in Fig. 2.
3.1. The 1994 Zanjiran earthquake
On June 20, 1994, an earthquake with an estimated
magnitude of M S 5.9, m b 5.9 occurred in the Firozabad
region in Fars province, in south Iran in the Zagros
Mountain Belt at 9:10:44 GMT (12:40:44 local time). The
maximum intensity IX (modified Mercalli Intensity Scale)
was reported in Zanjiran village. In spite of the vast
destruction of buildings, the number of causalities and loss
of life in this earthquake were very small. The earthquake
killed three people and injured 120. Maximum acceleration
of 10.98 and 10.04 m/s 2 for two horizontal components was
recorded at Zanjiran station (Table 2). The SH-wave
acelerogram records at Zanjiran, Zarat, Firozabad and
Maimand are shown in Fig. 2.
3.2. The 1999 Kareh Bas earthquake
On May 6, 1999 an earthquake with estimated magnitude
of M W 6.3 occurred near the Kareh Bas Fault (Fig. 3); 26
people were killed and more than 1300 buildings
were damaged. A maximum peak ground accelerations of
3.45 and 3.19 m/s 2 were recorded at the Dehballa station

624
H. Hamzehloo / Journal of Asian Earth Sciences 25 (2005) 621–628
Fig. 2. SH-wave accelerograms records from the 20 stations of the Iranian strong Ground motion array for the 1994 Zanjiran, the 1997 Ardebil, the 1999 Kareh
Bas, the 2002 Avaj, and the 2003 Jahrom earthquakes. The silent Feature for each station is given in Table 2.

H. Hamzehloo / Journal of Asian Earth Sciences 25 (2005) 621–628 625
Table 2
Strong ground motion recording stations
Earthquake Station Coordinate Horizontal peak ground acceleration
(m/s 2 )
8N 8E Elev. (m) Comp. L Comp. T
1994/6/20 Firozabad 28.86 52.61 1325 2.55 2.79
Maimand 28.87 52.75 1520 4.31 4.63
Zanjiran 29.07 52.62 1690 10.04 10.93
Zarat 29.10 52.30 1502 3.09 2.55
1997/2/28 Ardebil 1 38.25 48.30 1360 1.56 1.21
Ardebil 2 38.25 48.30 1360 1.64 1.20
Astara 38.48 48.88 K19 0.42 0.37
Namin 38.43 48.48 1450 0.67 0.96
Razi 38.63 48.08 1420 0.31 0.43
Sarab 37.94 47.53 1680 0.40 0.55
1999/5/6 Dehballa 29.28 51.93 750 3.19 3.45
Gavim 29.82 52.38 1800 0.38 0.33
Khanzeynan 29.66 52.10 1909 1.56 1.23
2002/6/22 Abegarm 35.75 49.28 1550 1.16 1.28
Avaj 35.58 49.22 1970 4.55 4.29
Abhar 36.15 49.22 1504 0.39 0.73
Darsajin 36.03 49.23 1675 0.55 0.75
Razan 35.38 49.03 1840 1.79 1.96
2003/7/19 Hajiabad 28.35 54.42 1030 3.58 2.91
Jouyom 28.25 53.98 840 0.70 0.43
(Table 2). The SH-wave acelerogram records at Dehballa,
Khanzeynun and Gavim are shown in Fig. 2.
3.3. The 1997 Ardebil earthquake
On February 28, 1997, an earthquake with an estimated
magnitude of M S 6.1, m b 5.5 struck a highly populated area
in northwest Iran at 12:57:12 GMT (16:27:12 local time).
The earthquake killed more than 1200 people and destroyed
12,000 buildings. The maximum intensity in Modified
Mercalli Intensity Scale reported for this earthquake was
VIII. Maximum accelerations of 1.56 and 1.21 m/s 2 for the
two horizontal components were recorded at Ardebil station
(Table 2). The SH-wave accelerogram records at Ardebil 1,
Ardebil 2, Astara, Namin, Razi and Sarab are shown in
(Fig. 2 and 4).
3.4. The 2002 Avaj earthquake
On June 22, 2002, a major earthquake, with an estimated
magnitude of M W 6.5, occurred near Avaj (250 km west of
Fig. 3. Fault plane solutions for the 1994 Zanjiran, the 1999 Kareh-Bas, and the 2003 Jahrom earthquakes given by HRV (gray) and this study (black).

626
H. Hamzehloo / Journal of Asian Earth Sciences 25 (2005) 621–628
Fig. 4. The fault plane solutions of the 1997 Ardebil earthquake given by HRV (gray) and this study (black).
Tehran) in NW Iran at 2:58:27.2 (GMT) (7: 28: 00 local
time). The earthquake killed over 226 people and injured
more than 1300. The earthquake was felt at Tehran and
affected 373 villages in Ghazvin, Hamedan, Zanjan, and
Markazi provinces. Maximum accelerations of 4.29
and 4.55 m/s 2 for the two horizontal components were
recorded at Avaj station (Table 2). The SH-wave accelerogram
records at Abegarm, Abhar, Avaj, Darsajin and
Razan are shown in Fig. 2.
3.5. The 2003 Jahrom earthquake
An earthquake with an estimated magnitude of M W 5.6
occurred on July 10, 2003 at 17:6:37 (GMT) in the Zagros
Mountains southeast of Jahrom in Fars province (Fig. 3).
The earthquake killed one person and injured 25. Maximum
peak ground accelerations of 3.58 and 2.91 m/s 2 for
two horizontal components were recorded at Hajiabad.
The SH-wave acelerogram records at Hajiabad and Jouyom
are shown in Fig. 2.
4. Results
The estimated causative fault parameters using SH-wave
data of recorded accelerographs for the 1994 Zanjiran earthquke,
the 1997 Ardebil earthquake, the 1999 Kareh Bas
earthquake, the 2002 Avaj earthquake and the 2003 Jahrom
earthquake are given in Table 3. The estimated strike, dip
and rake for the the 1994 Zanjiran earthquake using analyses
of SH-wave are 3358, 888 and K1368, respectively.
These values for the 1999 Kareh-Bas are estimated as
strikeZ1458, dipZ878 and rakeZK1608, respectively. For
the 1997 Ardebil earthquake the values of strike, dip and
rake are estimated as 1878, 858 and K108, respectively.
The fault parameters for the 2002 Avaj earthquake are
estimated as strikeZ1188, dipZ538, and rakeZ828, respectively.
These values for the causative fault of the 2003 Jahrom
earthquake are strikeZ3008, dipZ428 and rakeZ1188.
5. Discussion
5.1. The 1994 Zanjiran and the 1999 Kareh-Bas
earthquakes
The Harvard Centroid Moment Tensor (CMT) solution
gives values of strike, dip and rake for the 1994 Zanjiran
earthquake as 3438, 858, and K1578, respectively, while
the NEIC suggest values 3558, 608 and K1798 for strike,
dip and rake, respectively. It is observed that the values of
strikeZ3358, and dipZ888 from this study are in fair
Table 3
Estimated fault plane parameters using SH-wave analyses
Earthquake NP1
NP2
yy/mm/dd
Str Dip Rake Str Dip Rake
1994/6/20 335 88 K136 243 46 K3
1997/2/28 187 85 K10 278 80 K175
1999/5/06 145 87 K160 54 70 K3
2002/6/22 303 37 94 118 53 82
2003/7/19 300 42 118 84 54 67

H. Hamzehloo / Journal of Asian Earth Sciences 25 (2005) 621–628 627
agreement with strike and dip reported by Harvard (HRV)
and National Earthquake Information Center (NEIC). The
estimated rake of K1368 is close to the HRV than the
NEIC estimates. The focal mechanism, which was obtained
from analysis of SH-waves, shows right-lateral strike slip
motion.
Fault plane parameters, estimated for the causative fault
of the 1999 Kareh Bas earthquake, using analysis of
SH-waves, are 1458, 878 and K1608, respectively. The
estimated strike, dip and rake, as given by HRV, are 1438,
848, and K1658, respectively. The NEIC values for strike,
dip and rake are 1358,868 and K1798, respectively. Again a
fair agreement is observed between HRV estimates and
results obtained from analysis of SH-wave for strike, dip
and rake. The estimated rake is close to the HRV than the
NEIC estimates. A right-lateral strike slip mechanism is
observed from analysis of SH-wave.
The solutions for the 1994 Zanjiran and the 1999 Kareh
Bas earthquakes are in agreement with directions of
basement faults in the Zagros, which are aligned roughly
in a N–S direction (Fig. 3). Berberian (1976) concluded that
the focal mechanisms of these earthquakes would be strikeslip/
or normal faulting. The strike-slip motions on the
Kareh-Bas Fault and the causative fault for the Zanjiran
earthquake show strike-slip movement within a fold and
thrust belt. Strike-slip motion has been also reported by
Baker et al. (1993) on the Kazeron Fault.
5.2. The 1997 Ardebil earthquake
The estimated values of strikeZ1878, dipZ858, and
rakeZK108 from analysis of SH-wave are in fair agreement
with strike and dip reported by HRV and NEIC. The
Harvard Centroid Moment Tensor solution suggests values
of strike, dip and rake for the 1997 Ardebil earthquake as
1848, 578, and K158, respectively, while the NEIC suggest
values of 1828, 7608 and 178 for strike, dip and rake,
respectively. The focal mechanism, which was obtained
from the analysis of SH-waves, shows strike-slip motion for
the 1997 Ardebil earthquake.
5.3. The 2002 Avaj earthquake
The estimated strike, dip and rake from near field data are
1188, 538, and 828, respectively. NEIC and HRV have
analyzed far field broadband data to provide estimate of the
strike, dip and rake for the 2002 Avaj earthquake. NEIC
suggest a strike, dip and rake of 1178, 528, and 1018, while
the HRV gives values of 1028, 668, and 808 for strike, dip
and rake, respectively. It is noticed that the value of strike,
dip and rake from these two studies are in fair agreement
with the estimated strike, dip and rake from analysis of SH
waves of recorded near field data. The analyzes of SHwaves
suggest a reverse mechanism with left-lateral
component dipping toward SW.
Fig. 5. The fault plane solutions of the 2002 Avaj earthquake given by HRV (gray) and this study (black). The fault plane solution of the 1962 Buin-Zahra
earthquake is also shown.

628
H. Hamzehloo / Journal of Asian Earth Sciences 25 (2005) 621–628
These results are in agreement with tectonic situation in
this area. First, the Ipak Fault, which was responsible for the
1962 Buin-Zahra earthquake, has a reverse mechanism with
left-lateral component (Fig. 5) dipping toward the southwest
(Hessami et al., 2003). Secondly, the Soltanieh Fault shows
a dip toward the southwest (Fig. 5). Also, the 2002
Avaj earthquake, which occurred between the Ipak and
Soltanieh faults show reverse motion with dip toward the
southwest.
5.4. The 2003 Jahrom earthquake
The Harvard Centroid Moment Tensor (CMT) solution
suggest values of strike, dip and rake for the 2003 Jahrom
earthquake of 3058,428, and 1188, respectively, while NEIC
suggest strikeZ2988, dipZ478 and rakeZ1158. It is
observed that the values of strikeZ3008, dipZ428 and
rakeZ1188 from this study are in fair agreement with HRV
and NEIC estimates. The focal mechanism, which was
obtained from analysis of SH-waves, shows reverse motion.
The fault plane solution of the 2003 Jahrom earthquake
shows reverse faulting parallel to the local strike of the belt
and dipping towards north.
6. Conclusions
On the basis of analysis of SH-wave data for the 1994
Zanjiran, the 1997 Ardebil, the 1999 Kareh Bas, the 2002
Avaj, the 2003 Jahrom earthquakes the following conclusions
have emerged:
1. The SH-Waves analysis of near field accelerographs
can distinguish the fault plane from the auxiliary
plane. This method is especially helpful, when the
lack of information such as surface rupture, aftershocks
data and an isoseismal map make it difficult to
identify the causative fault plane in the HRV or NEIC
solutions.
2. The 1994 Zanjiran and the 1999 Kareh Bas earthquakes
show strike-slip motion with a approximately north–
south strike direction, which confirms the presence of
strike-slip motion in a folded and thrust belt. While the
2003 Jahrom earthquake shows reverse motion with the
fault plane parallel to the local strike of the belt and
dipping towards the north.
3. The 1997 Ardebil earthquake shows strike-slip motion
with an approximately north–south strike.
4. The 2002 Avaj earthquake shows reverse mechanism
with a fault plane dipping towards the southwest, which
is similar to the 1962 Buin-Zahra earthquake.
5. The estimated fault plane parameters from inversion of
the near field data based on the point source model for
these earthquakes are in fair agreement with solutions
given by HRV and NEIC.
Acknowledgements
I am grateful to International Institute of Earthquake
Engineering, and Seismology for supporting this research
work and Building and Housing Research Center, Tehran,
I.R. Iran for providing the strong ground motion data. I am
thankful to Dr John Milsom and Dr A.J. Barber for their
constructive comments on the manuscript.
References
Aki, K., Richards, P.G., 1980. Quantitative Seismology: Theory and
Methods, vol. 1. W.H.Freeman and Co, San Francisco.
Ambraseys, N.N., Melville, C.P., 1982, A., 1982. History of Persian
Earthquakes. Cambridge University Press, London.
Baker, C., Jackson, J., Priestley, K., 1993. Earthquakes on Kazerun line in
the Zagros mountains of Iran: strike-slip faulting within a folded-andthrust
belt. Geophysical Journal International 115, 41–61.
Berberian, M., 1976. Contribution to the seismotectonics of Iran (Part II).
Geological Survey of Iran, Report No. 39 1976;.
Berberian, M., 1979. Earthquake faulting and bedding thrust associated
with the Tabas-E-Golshan (Iran) earthquake of September 16, 1978.
Bulletin Seismological Society of America 69, 1861–1887.
Berberian, M., Papastamatiou, D., 1978. Khurgu (north Bandar Abbas,
Iran) earthquake of March 21, 1977: a preliminary field report and
seismotectonic discussion. Bulletin Seismological Society of America
68, 411–428.
Gutenberg, B., Richter, C.F., 1954. Seismicity of the Earth and Associated
Phenomena. Princeton University Press, Princeton, NJ.
Haskell, N.A., 1960. Crustal reflection of plane SH waves. Journal of
Geophysical Research 65, 4147–4150.
Hessami, H., Jamali, F., Tabassi, H., 2003. Major active Faults of Iran,
Scate 1:2,500,000, International Institute of earthquake engineering and
Seismology.
Jackson, J., Fitch, T., 1981. Basement faulting and the focal depth of the
large earthquakes in the Zagros mountains (Iran). Geophysical Journal
Research Astronomy Society 64, 561–586.
Jackson, J., Mckenzie, D.P., 1984. Active tectonics of the Alpine-
Himalayan Belt between western Turkey and Pakistan. Geophysics
Journal Research Astronomy Society 77, 185–264.
Kadinsky-Cade, K., Barazangi, M., 1982. Seismotectonics of southern Iran:
the Oman line. Tectonics 1, 389–412.
Kasahara, K., 1981. Earthquake Mechanics Cambridge Earth Sciences
Series. Cambridge University Press, Cambridge.
Lay, T., Wallace, T.C., 1995. Modern Global Seismology. Academic Press.
McKenzie, D., 1972. Active tectonics of the Mediterranean region.
Geophysical Journal Research Astronomy Society 30, 109–185.
Niazi, M., Basford, J.R., 1968. Seismicity of Iranian plateau and Hindukush
region. Bulletin Seismological Society of America 58, 417–426.
Ni, J., Barazangi, M., 1986. Seismotectonics of the Zagros continental
collision zone and comparison with the Himalayas. Journal of
Geophysical Research 91, 8205–8218.
Nowroozi, A.A., 1971. Seismo-Tectonics of the Persian plateau, Eastern
Turkey, Caucasus, and Hindu-Kush regions. Bulletin Seismological
Society of America 61, 317–341.
Nowroozi, A.A., 1976. Seismotectonic provinces of Iran. Bulletin
Seismological Society of America 66, 1249–1276.
Sarkar, I., Hamzehloo, H., Khattri, K.N., 2003. Estimation of causative
fault Parameters of the Rudbar earthquake of June 20, 1990 from near
field SH-wave Data. Tectonophysics 364, 55–70.
Shoja-Taheri, J., Niazi, M., 1981. Seismicity of the Iranian plateau and
bordering regions. Bulletin Seismological Society of America 71, 477–489.