Seismoprognosis Observations in The Territory of Azerbaijan: ISSN 2219-6641

ISSN 2219-6641
SEISMOPROGNOSIS OBSERVATIONS
IN THE TERRITORY OF AZERBAIJAN
Volume 16, № 2, 2019

http://www.seismology.az/journal
Republican Seismic Survey Center of
Azerbaijan National Academy of Sciences
INTERNATIONAL EDITORIAL
EDITORIAL BOARD BOARD
G.J.Yetirmishli (chief editor) A.G.Aronov (Belarus)

R.M.Aliguliyev (Baku, Azerbaijan) T.L.Chelidze (Georgia)
F.A.Aliyev (Baku, Azerbaijan) Rengin Gok (USA)
T.A.Aliyev (Baku, Azerbaijan) Robert van der Hilst (USA
F.A.Gadirov (Baku, Azerbaijan) Massachusetts)
H.H.Guliyev (Baku, Azerbaijan) A.T.Ismayilzadeh (Germany)
I.S.Guliyev (Baku, Azerbaijan) R.Javanshir (Great Britain)
T.N.Kengerli (Baku, Azerbaijan) A.V.Kendzera (Ukraine)
P.Z.Mammadov (Baku, Azerbaijan) A.A.Malovichko (Russia)
T.Y. Mammadli (Baku, Azerbaijan) Robert Mellors (USA Livermore)
H.O. Valiyev (Baku, Azerbaijan) X.P.Metaxas (Greece)
E.A.Rogozhin (Russia)
Eric Sandvol (USA Missouri)
L.B.Slavina (Russia)
N.Turkelli (Turkey)
Responsible Secretary: Huseynova V.R.

SEISMOPROGNOSIS OBSERVATIONS IN THE TERRITORY OF AZERBAIJAN, V. 16, №2, 2019, pp. 3-7 3
ASSESSMENT OF SEISMIC HAZARD IN THE TERRITORY OF

“TAKHTAKORPU” RESERVOIR OF AZERBAIJAN
G.J. Yetirmishli1, T.Y. Mammadli1, R.B. Muradov1, T.I. Jaferov1
Takhtakorpu reservoir and the relevant dam complex’s territories are located in the Darachay
valley (Takhtakorpu), 3.5 km south-west of Shabran. The area of the dam and reservoir is
characterized by smooth heights that are not too high, numerous ravines, complicated hills and
sloping plains. The absolute height of the surface is within 60-2500 m, here. There is Gaynarcha
mud volcano with an absolute height of 180 m in the abyssal mountain shore of Takhtakorpu river,
2 km from the dam. The volcano is located on the northern wing of the anticline with the same
name.
The tectonic elements of the northern part of the large Tangin-Beshbarmag anticline are
observed in the area1.5-2.0 km south of the Takhtakorpu reservoir.
The territory of the dam is within the north-eastern wing of the Gaynarcha anticline of the
Gusar-Davachi synclinorium. Gaynarcha anticline extends from north-west to south-east being 7
km width and 70-80 km length. The east extremity of the anticlinal folded have been exposed to
fault within the research area. The formation of the Gaynarcha mud volcano that is located 2 km
south-west of dam axis on the right bank of the Takhtakorpu river is associated with this fault.
The fault cannot harm the durability of the dam because the fault direction of the folding is
consistent with its way that means the fault is directed parallel at a great distance to the dam.
The Takhtakorpu reservoir is located in the north-eastern extremity of the Greater Caucasus
and this area isn’t seismically characterized by high activity. However, regularly occurrence of
relatively weak seismic shocks are observed here.
Directly, strong and destructive earthquakes have not been recorded in the research area till
now (Fig. 1). The strongest earthquakes occurred mainly in the north, west and south from the
Shabran region (Takhtakorpu reservoir) [1,2,3]. These earthquakes that are quite strong were felt at
high intensity certainly in the territory of Shabran district.
– The Takhtakorpu reservoir
Figure 1. Map of the strong earthquakes epicenters in the north-east of Azerbaijan during of 427-2018 years.
1
Republican Seismic Survey Center of Azerbaijan National Academy of Sciences
4 SEISMOPROGNOSIS OBSERVATIONS IN THE TERRITORY OF AZERBAIJAN, V. 16, №2, 2019, pp. 3-7
An analysis of the isoside schemes of the strongest earthquakes in Azerbaijan shows that an
earthquake with an intensity of 6 points on the MSK-64 scale has not been recorded in the
Takhtakorpu reservoir area of Shabran district until now. Seismic vibrations with this intensity is
mainly result of the earthquakes occurred in Shamakhi region. It should be noted that, only the
strong earthquake occurred in 1963 in the Caspian Sea was felt by the 7 point intensity in the
narrow territory along the coast of Shabran.
At first glance in Figure 1, the research area presents an asymmetric zone. But it is not so.
Epicenter map of earthquakes with M≥3,0 recorded in Azerbaijan and adjacent territories
during 1980-2018 [3]years indicates that there are small but weak seismic shocks in the research
area (Fig.2). Note that, recording of the large number of weak seismic shocks in Azerbaijan is
associated with the operation of digital seismic stations with very wide frequency-dinamic range in
Azerbaijan mainly since 2003, produced by the US , “Kinemetrics” company.
– Seismic stations
Figure 2. Earthquakes with ml>3 recorded in Azerbaijan and adjacent territories during the period 1980-2018 years.
As mentioned above, earthquakes maximum with magnitude intensity 6 on the scale MSK-64
has been recorded in the territory of Shabran district till now. Seismic vibrations with this intensity
are mainly result of the earthquakes in Shamakhi region. Just the strong (M=6.2) earthquake [4]
occurred in the Caspian Sea in 1963 year had been felt at the 7-point intensity in the narrow area
along the seashore of the Shabran district.
However, the result obtained by these observations doesn’t mean that the earthquakes with the
more intensity will not occur in the Shabran region in the future. To determine the spatial position
of potential source zones in the territory of Azerbaijan, abundance (both lateral and vertical) of the
strong and weak earthquakes on the point of this area and relation of the large depth faults with the
zones of the tense concentration of the seismic shocks have been investigated [5,6].
It is clear from research that, strong earthquakes occur not everywhere but in the areas where weak
earthquakes are concentrated. Based on this factor, T. Mammadli developed a method for
identifying source zones of strong earthquakes based on weak earthquake concentrations [5,6]. This
method, unlike the methods used so far in seismoactive areas, allows for the detection of potential
seismic hazards in seismoactive areas before any fault zone and seismic data of strong
earthquakes,in advance, without pre-adapting to any fault zone and seismostatistic data of strong
G.J. Yetirmishli et al: ASSESSMENT OF SEISMIC HAZARD IN THE TERRITORY OF “TAKHTAKORPU” ... 5
earthquakes. The application of the method revealed that there are numerous and various sizes of
active fault zones (or potential source zones) in the territory of Azerbaijan (Fig.5).
The spatial position of these fault zones shows that the seismic area of Azerbaijan Republic
has a mosaic structure.
Figure 3. Scheme of seismic and strong earthquake zones of the Azerbaijan Republic
Conventional signs:
– epicenter of earthquake; – Seismic stations;
– active fault or potential source zones;
In order to identify the characteristics of the earthquakes distribution on depth, the seismic
sections on II-II profiles with the south-west and north-east directions and I-I profiles with the west-
east directions have been compiled in the research area (Fig.5 and 6)
Figure 4. Location map of profiles I-I and II-II

I-I profile
II-II profile
Figure.5. Seismological transects by profiles
As can be seen seismic transects, seismic shocks are densely concentrated mainly in the west
and south-west part which corresponds to the Shamakhi-Ismayilli zone of transects. Although these
hypocenters are from 3km to 20-25 km depth but the depth of some shocks is 40-45 km. Strong
earthquakes(M≥5,0) occur in the depth (10-15 km) near the surface of the crystalline foundation
here, as in other parts of the Greater Caucasus. Note that, the number of weak seismic shocks is low
in 40km depth in these parts even though it is observed that they tend to occur frequently. The
strong (M = 5.3) earthquake (M=5.3) had been occurred on October 7, 2012 in Ismayilli, at this
depth. Interestingly, the strong earthquake (M = 5.8) occurred on February 10, 2014 in Hajigabul at
the same depth. For this reason, it is considered expedient that investigate more extensively the
manifestation features of seismicity at such depth in these areas in future.
Although the number of seismic shocks decreasing gradually to the east and north-east by
section, it is observed that they tend to occur frequently at the 10-15 km and 40-45 km depth in
separate parts of the area.
As you can see from Fig.4, active faults with Caucasian direction that is larger than the
surrounding source zones and anti-Caucasian direction or potential source zones is different from
others. The maximum magnitude (Mmax) of probable earthquakes in these source zones have been
determined in [6] and they are M max = 7.4 and Mmax = 6.7, respectively. near the research area active
It is possible to determine the macroseismic effect created by the probable strong earthquakes
in these source zones on the surface using the assessments of coefficients of macroseismic field
equation [8] that assigned by F.T.Guliyev for this region and macroseismic field equation that
assigned by N.V.Shebalin [7].
G.J. Yetirmishli et al: ASSESSMENT OF SEISMIC HAZARD IN THE TERRITORY OF “TAKHTAKORPU” ... 7
The conducted calculations show that, if maximum magnitude earthquakes occur in the
above-mentioned potential source zones, seismic hazards with an intensity of 8-9 points on the
MSK-64 scale may occur in the “Takhtakorpu” reservoir area where the research is being
conducted.
Conclusion
1. The Takhtakorpu reservoir area is not seismically characterized by high activity. No
earthquake with a magnitude greater than 6 on the MSK-64 scale has been recorded so far
,here. The seismic vibrations with this intensity are mainly spread by earthquakes in
Shamakhi region.
2. Researches show that, there are two sufficiently large-sized active faults (or potential source
zones ) in the area near the reservoir. According to calculations, the probable earthquakes
with maximum magnitude in the such source zones can create seismic hazard with 8-9 point
intensity on the MSK-64 scale in the territory of Takhtakorpu reservoir.
REFERENCES
1. Новый каталог сильных землетрясений на территории СССР / Отв. редактор Н.В.

Кондорская, Н.В.Шебалин. М.: Наука, 1977, 535 с.
2. Землетрясения в СССР в ….году (ежегодники 1976-1991гг)
3. AMEA nəzdində Respublika Seysmoloji Xidmət Mərkəzinin fondu (1992-2018-ci illər üzrə
zəlzələlər kataloqu)
4. Рагимов Ш.С. Каспийское землетрясение 27 января 1963 года Вопросы изучения
строения Земли. Баку, Изд. АН Азерб. ССР, 1966, с.153-155.
5. Маммадли Т.Я. Выявление очаговых зон сильных землетрясений Азербайджана и
определениe их максимальных магнитуд (Mmax) по слабой сейсмичности. Azərbaycan
Milli Elmlər Akademiyası Xəbər-lər Yer elmləri №4, 2005, s.60-64
6. Маммадли Т.Я Новая методика выявления очаговых зон сильных землетрясений и
определение их максимальных магнитуд (Mmax) по слабой сейсмичности (на примере
территории Азербайджана). ПРОБЛЕМЫ СЕЙСМОТЕКТОНИКИ. Материалы XVII
Всероссийской конференции с международным участием 20-24 сентября 2011 года,
Воронеж-Москва, 2011, с337-341.
7. Шебалин Н.В. Очаги сильных землетрясений на территории СССР. М.Наука,1974,
53с.
8. Кулиев Ф.Т. Уравнение макросейсмического поля для Азербайджана и его
геотектонических областей. Сейсмологический бюллетень Кавказа, 1987. Тбилиси:
Мецниереба, с.129-140.
ANOMALOUS CHANGES OF MAGNETIC FIELD BEFORE

THE ZAGATALA EARTHQUAKE ON 05.06.2018
A.G.Rzayev1, L.A. Ibrahimova1, N.B. Khanbabayev1, M.K. Mammadova1, V.R. Huseynova1
Introduction: Researchers know that the strong earthquakes in seismoactive areas are
frequently accompanied by geomagnetic effect. Magnetometric investigations allow in many cases
can help to clarify boundaries of geological structures (Rzayev, 2006; Yetirmishli et al. ,2013).
The accumulation of stress-strain energy at the different depths of the Earth is related to local,
ionosperic and cosmogenic factors (Finkelstein et al., 2012). Mechanical, physico-chemical and the
other features of the environment of the earthquake sources in the area of the north and southern
slopes of the Greater Caucasus, Kura Depression and Lesser Caucasus where anomalous stress-
strain energy is accumulated, changes with characteristic features. Effects of the such active
processes on the surface are studied in the seismoactive regions of the world as the earthquake
warning factors and geophysical areas: gravitational, electrical, magnetic and geochemical
anomalous changes. [1,2,3]
The first information about earthquakes in the north-western region of Azerbaijan in the
Greater Caucasus dates to 1850 year. Strong earthquake in the region occurred in 1936 and 1948
years (m l≥5) ( Aghamirzoyev, 1987). In the recent years, the earthquake with magnitude of 7 is
occurred on 07.05.2012 in the Zagatala-Balakan zone (ml = 5,6 h=9 km φ = 41,50ºN, λ = 46,58ºN)
and in the Zagatala area in 2018 year.
The earthquake with 10 km depth and magnitude of 5.5 had been occurred in the Zagatala
region on 05.06.2018. In the article, the mechanism of the earthquake source is mentioned as a main
factor in the occurrence of the seismic events as a warning element of anomalous seismic effects.
According to the results of observations of the geomagnetic regime, there is detailed information for
the interpretation and analysis of the characteristic gradient and increasing of the geomagnetic field
tension , during the preparation of seismic event at the Shamakhi-Sheki-Balakan geodynamic
polygon.
It can be noted that the coverage of the Zagatala earthquake area is in the southern sunset of
the Greater Caucasus mega anticlinorium from a geological perspective (Pleistocene zone).
This can be evaluated as Zagatala tension zone. This zone is surrounded by the west of
Gasakh-Signakh fault and to the east by the Ganjachay-Alazan fault (Shikhalibeyli et al. 1978).
The area in the magnetic field is recorded to as the Shamkhor-Zagatala transverse magnetic
anomaly. Within this anomaly, two large significant positive magnetic anomalies are distinquished:
Alazan and Gutan (Metaxas, 1979).
These large-scale anomalies are located in the intersection zone of the lengthwise Caucasus
and transverse tectonic structure. These anomalies are considered as the elements of the
Anticaucasus megazone. The Alazan and Gutan anomalies are characterized by strong magnetic
field gradient, which is indicated in the south and north directions. Such zones can be considered as
normal fault characteristic areas.
The depth of the upper layer of the excited magnetic mass of the Guton magnetic anomaly is 2
km, and for the Alazan magnetic anomaly is 4 km (Метaxas, 1979). Thus, these anomalies
belonging to the Alpine basis area are of the highest level and this area is considered as a high risk
area.
It should be noted that, the rise of the foundation up to Alpine in the transverse Shamkhor-
Zagatala sructure and being closer of thrust to the surface are the basis of seismic events in this
area. The seismicity of this area that is characteristic of normal fault depend on the being the
lengthwise blocks up to Alpine with the south-north direction and the effect of transverse
1
A.G.Rzayev et al: ANOMALOUS CHANGES OF MAGNETIC FIELD... 9
movements. There are also seismogenic slip-strike structure elements in parallel with the normal
fault in the foundation up to Alpine exposed benching grounding directed to the east from the
Ganja-Alazan transverse fault.Thus, it is thought that, the earthquake occurred in Zagatala city to
have a direct relationship with the presence of transverse and cross-section faults in the movements
of Earth’s crust along with the formation of a geodynamic regime. In addition to above mentioned,
the main cause of earthquakes in this area is presence of the Gazakh-Signakh and Ganja-Alazan
right-sided faults.
The purpose of the research: coordinates of the Zagatala earthquake occurred on 05.06.2018
was φ = 41.50ºN, λ = 46.67 ºE, magnitude was ml = 5.5 and the depth of the source was h = 10 km.
The coordinates of this earthquake are partly consistent with the earthquake coordinates
occurred in 2012 year (φ = 41.56ºN, λ = 46.63 ºE; ml = 5.7; h = 12 km) - (Rzayev, Metaxas, 2012).
It is advisable to provide detailed information about the earthquake with the magnitude of 5.5
in the city of Zagatala. Changes in seismomagnetic effects in Sheki city and Ismayilli city points
have been continously monitored a month before the seismic event, in the time of the event and a
month after the event .Geomagnetic observatons at both these sites were observed at the
background level month ago.
Abnormal changes caused by strong earthquakes occurred in the Shamakhi-Sheki-Zagatala-
Balakan zones, estimated by high seismic risk and geodynamic activity are recorded by modern
geophysical devices installed on the seismic stations data are transmitted to RSSC. The data is
operatively analyzed and the change graphs depending on the time of seismomagnetic effect are
created. Changes of the seismomagnetic effect have been remarkable before and after the strong
Zagatala earthquake.
Figure 5. Mechanism of the Zagatala earthquake (ml=5.5) on June 5, 2018 year (with the extension character)
(compiled by S.E.Kazimova)
This indication proves that the geodynamic regime of the seismogenic zone of Zagatala
didn’t changed which was determined by the movements of blocks on the Earth’s crust in relation
to the cross-section and transverse faults. The mechanism of the earthquake occurred on 05.06.2018
is estimated as a left-sided normal fault component. It is supposed that it is mainly formed by the
right-sided movements of the Gazakh-Signakh and Ganjachay-Alazan zones (Rzayev and Metaxas,
2012).
Geomagnetic observations have been formed due to increments 10 days before the event and
have been increased to a maximum value of 20÷30 nT. This process continued 10 days after the
gedoynamic event.
As can be seen from the compiled curve, the seismomagnetic effect have been observed with
the chaotic oscillations of 20÷25 nT and it have been continued with increases. In both sites, the
changes of seismomagnetic effects have been occurred during the earthquake (Fig.2).
Stm/st Ismayilli (May, June, July)

t day
Figure 2. Manifestation of seismic effect of the Zagatala earthquake occurred in 2018 year.
The spatial-time increase in the geomagnetic field tension have been analyzed and allowed us
to assess the regularity of dependence on seismic activity.
As can be seen from the created map, seismomagnetic effect is quite in the Gabala –Ismayilli
geodynamic polygon, whereas the geodynamic field tension in the Balakan-Sheki is more active.
The maps complement one another.
In the map created in 3D format, the increases are remarkable in the effect due to geodynamic
field in the Balakan-Sheki polygon.
In the map created in 2D format, it is specifically mentioned that the complexity of the 50-100
nT values by closing of isometric line of the geomagnetic effect observed by seismic activity in the
Qabala-Ismayilli zones (Fig. 3)
A.G.Rzayev et al: ANOMALOUS CHANGES OF MAGNETIC FIELD... 11
Figure 3A. Tension-deformation condition of geological environment based on the magnetic data
observed in the Sheki-Shamakhi polygon (in 3D format, June 2018).
Figure 3B. Tension-deformation condition of geological environment based on the magnetic data
observed in the Sheki-Shamakhi polygon (in 2D format, June 2018).
Conclusion
Analysis of the source mechanism and the module of the full vector of T temporal variations,
spatial-time variations of geomagnetic field tension gradient, the dynamics of the tension-
deformation conditions generated in the Shamakhi-Sheki-Balakan polygon have been clarified. It
was accepted as a warning factor of the seismoanomal geomagnetic effects revealed before the
Zagatala earthquake with ml = 5.5 occurred on 05.06.2018.
REFERENCES
1. Рзаев А.Г., Етирмишли Г.Д., Казымова З.Е 2013. Отражение геодинамического режима в
вариациях напряженности геомагнитного поля ( на примере склона Большого Кавказа).
AMEA “Xəbərlər” Yer Elmləri, №4, с. 3-15 (рус).
2. Рзаев А.Г 2006. Связь аномальных изменений в напряженности геомагнитного поля с
сейсмотектоническми процессами в литосфере Земли. AMEA “Xəbərlər” Yer Elmləri, №3,
с. 58-63 (рус).
3. Рзаев А.Г., Метаксас Х.П 2012. Загатальские землетрясения 7 мая 2012 года; Загадки
геодинамического режима и сейсмомагнитный эффект. AMEA RSXM. Azərbaycan
ərazisində seysmoproqnoz müşahidələr. Стр 362-371.
4. Метаксас, 1979. Методика и результаты интерпретации материалов магнито разведки при
изучении мезозойской эпохи Средне Куринской впадины. Канд. Дис.
5. Ин-т Геофизики АН Груз. ССР, Тбилиси.
6. Шихалибейли Э.Ш. Тагиев Р.Э. Метаксас Х.П. 1978 Поперечные разрывы Западного
Азербайжана. Изв. АН АзССР, Серия наук о Земле, №5, с.35-41.
7. Агамирзоев Р.А. Сейсмотектоника Азербайджанской части Большого Кавказа, «Элм»
Баку 1987.
1D VELOCITY MODEL BY LOCAL EARTHQUAKE DATA
S.E. Kazimova1, Sh.N. Khadiji1, S.E. Gummatli1
Introduction
In this study, one-dimensional (1-D) P- and S-wave velocity structures of upper crust in the
Azerbaijan region and precise hypocentre locations are recorded by the Republican Seismic Survey
Centre’s stations, during the period 2003 – 2018. We performed an analysis to find the best P-wave
one-dimensional velocity model for the crystal structure of the study area, using the VELEST
algorithm. We used 5423 P- and 4478 S-arrival times of 2650 events recorded at 30 stations. We
found eleven distinct layers within the upper 60 km of the crust. We studied the area from
seismological and geological point of view and we analyzed the influence of the velocity model on
the earthquake locations. We analyzed the instrumental seismicity of the Middle Kura Depression
region recorded by the Republican Seismic Survey Centre’s stations, during the period 2003 –
2009[9]. We used standard seismological methods to compute the Vp/Vs ratio, one-dimensional
velocity model, and station corrections for earthquake relocations.
Earthquake location can be improved using a reference 1D model close to the true earth
model and station corrections that mitigate the effects of the structure close to the receiver and
deviations from the simple, homogeneous model. Kissling proposed that the natural solution to this
problem is the least square solution. They called this solution the minimum 1D model. Following
this approach, we first established the starting 1D models using the available information on the
crystal structure. Starting velocity values were selected considering available data and the results of
Gasanov A.(1989)[1]. We used four layers each for the crust and the uppermost mantle for a total
of eight layers.
COUPLED HYPOCENTER VELOCITY MODEL PROBLEM
The travel time of a seismic wave is a non-linear function of both hypocentral parameters and
seismic velocities sampled along the ray path between station and hypocenter. This dependency of
hypocentral parameters and seismic velocities is called the coupled hypocenter-velocity model
problem (Crosson 1976, Kissling 1988, Thurber 1992)[4, 9]. It can be linearized and in matrix
notation is written as (Kissling et al. 1994):
t = Hh + Mm +e = Ad + e,
t vector of travel time residuals (differences between observed and calculated travel time); H
matrix of partial derivatives of travel time with respect to hypocentral parameters; h vector of
hypocentral parameter adjustments; M matrix of partial derivatives of travel times with respect to
model parameters; m vector of velocity parameter adjustments; e vector of travel time errors,
including contributions from errors in measuring the observed travel times, errors in the calculated
travel times due to errors in station coordinates, use of the wrong velocity model and hypocentral
parameters, and errors caused by the linear approximation; A matrix of all partial derivatives; d
vector of hypocentral and model parameter adjustments.
In standard earthquake location algorithms the velocity parameters are kept fixed to a priori
values - that are assumed to be correct - and the observed travel times are minimized by perturbing
hypocentral parameters. Neglecting the coupling between hypocentral and velocity parameters
during the location process, however, can introduce systematic errors in the hypocenter location.
Furthermore, error estimates strongly depend on the assumed a priori velocity structure. Precise
hypocenter locations and error estimates, therefore, demand the simultaneous solution of both
velocity and hypocentral parameters. The optimal 1D model will be achieved by simultaneously
inverting for hypocenter and velocity parameters [10]. The minimum 1D velocity model obtained
1 Republican Seismic Survey Center of Azerbaijan National Academy of Sciences

by this trial-and-error process represents the velocity model that most closely reflects the priori
information obtained by other studies, e.g. refraction studies, and that leads to a minimum average
of RMS values for all earthquakes.
BUILDING A 1D VELOCITY MODEL: DATA SELECTION AND INITIAL MODEL
We performed an analysis to find the best P-wave one-dimensional velocity model for the
crystal structure of the study area, using the VELEST algorithm [9]. This approach incorporates
iterative simultaneous inversion of hypocenters and 1-D velocity model.
The calculation of a minimum 1D model requires a set of well constrained events.
Uncertainties in hypocenter locations will introduce instabilities in the inversion process, because of
the hypocenter-velocity coupling. The largest azimuthal gap of observations (GAP) and the
minimum number of observations per event are very good criteria to reliable and robust earthquake
locations [5-8]. This reduces the data set used for the P-wave inversion to a total number of 2650
events.
After 9 iterations, we obtained a variance improvement of about 86%, and a final RMS of 4.2
s. The computed P and S-wave 1D-velocity model is shown in Fig.1 with red lines.
Figure 1. Final 1D velocity models after 9 iterations by Velest program
S-wave phases add important additional constraints on hypocenter locations because partial
derivatives of S-wave traveltimes are always larger than those of P waves by a factor equivalent to
VP/VS and they act as an important constraint within an epicentral distance of 1.4 focal depths. The
use of S waves will in general result in a more accurate hypocentre location, especially regarding
focal depth. On the other hand, a large S arrival time errors at a station close to the epicentre can
result in a stable solution with a small RMS, but is actually significantly mislocated even for cases
with excellent azimuthal station coverage.
A schematic 1D model used to approximate the unknown velocity structure for earthquake
location and used as the reference model for 3-D tomographic inversions is shown in Fig.2.
S.E. Kazimova et al: 1D VELOCITY MODEL BY LOCAL EARTHQUAKE DATA 15
Figure 2. Final schematic 1D velocity model
Discussion
Figures- 3 and- 4 show the final and preliminary locations respectively of 2650 events.
Average differences between final and preliminary locations in latitude, longitude, depth and origin
time are ±5-10 km, ±5-10 km, 6-11 km and 2 ± 4 s, respectively. The shifting of the hypocentres
systematically in one direction, for example focal depth, is a good test for the robustness of a
minimum 1-D model. The systematic shift is on the order of ±5-10 km in longitude. This eastward
shift is likely due the N–S linear array orientation of the RSSC network. The depth values of final
locations indicate that the majority of events occur between 5 and 10 km for the region, while
preliminary locations have both more shallow and also deeper events.
Figure 3. Difference in latitude and longitude between the first location(a) and Velest relocation(b)
After shifting all events to a greater depth by 10 km, two inversions were performed, one with
slightly damped and one with strongly overdamped velocities, the results of which are shown in
Fig.5, respectively. Since we have solved a coupled hypocentre–velocity problem, the initial bias in
the hypocentres may be compensated by adjusting the velocities, or by relocating the events to their
original position, or by a combination of these methods.
Figure 4. Difference in origin time between the first location(a) and Velest relocation(b)
We note a consistent decrease of RMS values for the relocated earthquakes. Moreover,
residuals at the stations within 180 km of the epicenter are greatly reduced. Although hypocentral
errors are for some cases larger with the new model, we are satisfied with the relocations, because
of the reduction of RMS and the fit of P-wave arrivals at close distance from the epicenter.
Conclusions
This paper has focused on the simultaneous determination of the 1-d P- and S-wave velocity
models in the Middle Kura depression, Central Azerbaijan, using the travel time inversion
algorithm Velest. We have created a more accurate and stable 1-d P- and S-wave velocity models
which give rise to new locations of aftershocks with minimum errors in RMS values and station
corrections for the P- and S-wave arrival times. It is found that the P-wave velocities are quite low
(<10 km/s) for the 12 km thick unconsolidated sediments of the Middle Kura depression. The P-
wave velocity at a depth of 12 km increases to nearly twice that of the upper sedimentary layer.
This result is consistent with the P-wave velocity model obtained by the results of 3-d seismic
tomography given by Gasanov A.G. (1989). The P-wave velocity value reaches to 6.3 km/s from 10
to 25 km depth with an increasing gradient a thick layer was defined with a P-wave velocity of 7.2
km/s at depth range of 25-45 km [2].
After several tests and trial solutions, 1-D S-wave velocitiy model was obtained for the
optimum values of VP/VS ratio. Although, the VP/VS ratio is very low at shallow depths (<10 km),
it gradually decreases in the layers deeper than 10 km. The sudden increase of the VP/VS ratio at 2
km depth is consistent with a high P-wave velocity at that depth.
Several tests on the stability of final velocity model prove that the final 1-D P- and S-wave
velocity models found in this study represent the most acceptable model for future relocation
processes in the area. Graphical patterns of RMS residuals, depth, latitude, longitude and depth
using the new crustal velocity model confirmed that the event locations have been improved.
REFERENCES
1. Гасанов А.Г., Глубинное строение и сейсмичность Азербайджана в связи с прогнозом

нефтегазоносности, Баку: Элм, 2001 г., с. 166-187.
2. Казымова С.Э. Изучение скоростной модели земной коры по цифровым сейсмоло-
гическим данным. // Gənc Alimlərin Əsərləri, № 1, AMEA, Bakı, 2008 г., c. 205-211
3. Sandvol, E., Al-Damegh, K., Calvert, A., Seber, D., Barazangi, M., Mohamad, R., Gok, R.,
Turkelli, N., and Gurbuz, C. Tomographic imaging of Lg and Sn Propagation in the Middle
East //Pure and Applied Geophysics, 158, 1121-1163, 2001.
S.E. Kazimova et al: 1D VELOCITY MODEL BY LOCAL EARTHQUAKE DATA 17
4. Jost M.L., Herrmann R. A student's guide to and review of moment tensors // Seism. Res.
Lett. 1989. V. 60. P. 37-57.
5. Yetirmishli G.J., Kazimova S.E., Kazimov I.E. One-dimensional velocity model of the
Middle Kura depresion from local earthquakes data of Azerbaijan // Fizika Zemli, 2011, No.
9, pp. 103–112.
6. Yetirmishli G.J., Kazimova S.E., The velocity model of the earth crust of Azerbaijan
according to digital seismic stations // The Geology and Geophysics of the South Russia,
№1/2012, ISSN 2221-3198, pp. 59-73
7. Kazimova S.E., The velocity model of the Middle Kura depresion earth crust from body
waves - Diss.. Philosophy. doctor. of geolog.-miner. Sciences, Baku, 2012 y, 160 p.
8. Kazimova S.E., Kazimov I.E. Seismic anisotropy under the southern slope of the Greater
Caucasus, PROCEEDINGS. The Sciences of Earth, 2011, № 3
9. Kissling E., W.L.Ellsworth, D.Eberhart-Phillips, U.Kradolfer Initial reference models in
local earthquake tomography // JGR. 1994. V.99, N.B10, P.19,635-19,646, Oct. 10.
10. Kissling E. Geotomography with local earthquake data. Res // Geophys., No 26, 1988,
р.659-698.
ASSESSMENT OF MODERN GEODYNAMICS OF AZERBAIJAN

BY GPS MEASUREMENT DATA
G.J.Yetirmishli1, I.E. Kazimov1, A.F.Kazimova1
Introduction
From the standpoint of plate tectonics, the existence of any lithospheric plate gives rise to
certain geological processes at its borders. The nature of these processes, first of all, depends on the
type of interaction with neighboring plates, in other words, on the type of interplate boundary. In
turn, the type of interaction between the plates is determined by the directions and velocities of their
movements, that is, their kinematics. Over time, the kinematics of lithospheric plates were
determined using paleomagnetic, paleoclimatic, geological, geomorphological, seismological
research methods that record the effects of plate interactions and their movements. Over the past
decades, space geodesy methods have been actively developed, which make it possible to determine
the location of objects on the Earth's surface with high accuracy. Changes in the position of such
objects in time tell us about their kinematic characteristics. GPS satellite positioning system, at the
moment, is the most developed among such systems. It has the necessary resolution for the
quantitative assessment of a wide range of geological processes and, including, to identify the
processes themselves. The use of satellite geodesy methods made it possible for a new approach to
determine the motion parameters of lithospheric plates. Based on the results of GPS measurements,
employees of the Massachusetts Institute of Technology built new models of instant kinematics of
Mediterranean and Caucasian region plates (Fig. 1 a, b).
Figure 1a. Simplified topographic/bathymetric (SRTM30 PLUS; http://topex.ucsd.edu/WWW_html/

srtm30_plus.html) and tectonic map of the study area, including the zone of interaction of the Nubian,
Somalian, Arabian, and Eurasian plates. Abbreviations are North Anatolian fault (NAF), East Anatolian fault
(EAF), Dead Sea fault (DSF), Mosha fault (MF), Pembak-Sevan-Sunik fault (PSSF), Tabriz fault (TF),
Chalderan fault (CF), Gulf of Corinth (Cor), Peloponnesus (Pe), Aegean (Aeg), Lesser Caucasus (LC),
Cyprus trench (Cyp), Karliova Triple junction (KT), Sinai (Sin), Caspian Sea (Cas), Main Caucasus Thrust
(MCT), East African rift (EAR), Kopet Dag (Kop), Apsheron Peninsula (AP), Alborz Mountains (Al).[7]
Figure 1b. Map showing decimated GPS velocities relative to Eurasia determined in this study. For clarity,
we plot 1s velocity uncertainties (see Table S1 for a complete tabulation of the velocities determined in
this study). [7]
1
G.J. Yetirmishli et al: ASSESSMENT OF MODERN GEODYNAMICS OF… 19
As you know, Azerbaijan is part of the Alpine-Himalayan mountain belt, formed in the
Cenozoic on the southern edge of the East European platform as a result of a collision between the
Eurasian and Arabian plates, which over the past five million years has experienced a rapid rise.
The advance of the Arabian (also called Arab) plate to the north is partially offset by the
displacement of the Anatolian block to the west. The tectonics of this vast region are mainly
determined by the collision of the Arabian and African plates with the Eurasian plate. Models based
on the global analysis of data on the movement of various plates show that, relative to the Eurasian
plate, the Arabian plate moves in the north-north-west direction at a speed of about 18-25 mm / year
(averaged over the past 3 million years). The African plate moves north with a lower speed of 10
mm / year, which causes a left-side shift along the zone of the Dead Sea faults. The advancement of
the Arabian Plate to the north is also responsible for the formation of the Zagros mountain structure,
the formation of the high plateaus of Eastern Turkey and the growth of the mountain structures of
the Lesser and Greater Caucasus [3, 7].
The aim of our research was to calculate the velocities of modern horizontal displacements of
individual tectonic blocks throughout the republic and to analyze their influence on strong
earthquakes that occurred in 2017 and 2018.
Methods of studying horizontal modern movements of the surface of the Earth's crust
The study of modern movements and deformations occurring in the massif requires the
monitoring mode of high-precision geodetic measurements of the displacements of the benchmarks
of specially equipped observation stations - geodynamic ranges [1].
In the past few years, in our Center (RSSC), along with traditional geodetic observations,
methods of satellite geodesy have been used. The combination of traditional ground-based and
satellite measurements allows us to quite successfully solve the tasks. Due to its high performance,
satellite technologies made it possible to obtain information on deformations of the Earth's surface
at bases from a few meters to several tens of kilometers with high frequency, which was difficult
using traditional measurement methods and, very important, to ensure the safety and efficiency of
mining. To carry out satellite geodetic measurements, 24 GPS-receivers of the geodetic class from
Trimble were used [2,4].
Thus, in the study of geodynamic processes using GPS technologies, two spatio-temporal
modes are mainly used for a one-time redefinition of the initial coordinates of points of geodetic
networks, and displacements of the reference values of deformations [5].
The data obtained as a result of experimental work on the current stress-strain state of the
Earth's crust and the patterns of its change in time, on the one hand, provide new fundamental
knowledge about the nature of the natural deformation processes that occur in the upper part of the
Earth's crust and the effect on the formation of a stress state.
Azerbaijan's geodynamics assessment based on GPS measurements for 2017-2018 years

In recent years, Azerbaijan has been characterized by active seismic activity, in which the
accumulated tension in the collision zone is released. In general, the seismic activity of the territory
of the republic in 2017 varies in the range of 0.2-0.6. As in previous years, the maximum values
were noted in the Gabala, Shabran and Shamakhi-Ismayilli districts (A = 1.0-2.0). However, it
should be noted that the seismic activity of the Kura Depression in the Saatli and Agdam regions
has increased. On May 11 at 07:24:19 in the Saatli region there was an earthquake with a magnitude
of 5.3 and felt up to 4-3 points. On November 15, local time, 23:48:02 in the region of Agdam, an
earthquake occurred with ml = 5.7 felt up to 6 points. The area of constant released tension, where
in the absence of strong earthquakes many weak ones occur - the Talysh region, as in previous
years, is characterized by maximum seismic activity (A = 1.6-2.0) [8].
In 2018, 16 tangible earthquakes with Мl = 3.2–5.5 occurred in the study area. Two
significant earthquakes with Мl> 5.0 were recorded, which were felt at the epicenter with intensities
of 5 and 6 points. Increased seismicity was observed in the Talysh mountain region, where there
were 6 tangible earthquakes with Ml = 3.4 - 5.0, which were felt at the epicenter with an intensity of
3 to 5.5 points.
Based on said above, we analyzed the data of GPS stations for 2017-2018 years. The velocity
estimates are based on the analysis of the time series of GPS station coordinates calculated from the
primary data, which are sets of phase and code measurements at two frequencies lasting 24 hours
with a recording interval of 15 s.
Thus, horizontal speed maps were constructed according to the data of the geodetic network
of GPS stations in Azerbaijan for 2017 and 2018 years. (Fig. 2,3). As the analysis of the velocity
distribution shows, the average values of the velocities of horizontal displacements of points to the
north and east are not constant, and the processes of shortening the surface of the Earth's crust in the
study region are also not constant. In addition, strong tangible earthquakes that occurred during
these periods were plotted on the map. As can be seen in the Figure 2, the maximum values of the
horizontal movements of individual blocks are characterized by increased seismic activity.
Detected increase in velocity in 2017-2018 years at Lerik, Lankaran, Jalilabad, Agdam and
Saatli stations (Fig. 4), compared with other years, is the most significant feature of the velocity
field in the study region. On the comparative velocity chart between 2017 and 2018 years (Fig. 4) a
direct proportional dependence is observed. In addition, over the course of these two years, the
speed value at Gusar station has noticeably decreased.
In conclusion, it should be noted that the use of modern methods of traditional and satellite
geodesy for observing the process of movement of the Earth's surface allows us to conduct research
at a qualitatively higher level. The results of the studies, as well as the GPS measurement data, can
be used to determine the kinematics of lithospheric plates, identify and clarify their boundaries, in
the zone of influence of which are located sources of strongest earthquakes, to highlight the main
fault systems and the most seismically dangerous zones, to track the progress of the change of
stress-strain state of the environment and the accumulation of elastic deformations in the zones of
such faults.
Figure 2. Velocities of horizontal movements of the Earth's crust surface according to the data
of the geodetic network of GPS stations in Azerbaijan in 2017
G.J. Yetirmishli et al: ASSESSMENT OF MODERN GEODYNAMICS OF… 21
Figure 3. Velocities of horizontal movements of the Earth's crust surface according to the data
of the geodetic network of GPS stations of Azerbaijan for 2018
Figure 4. Comparative graph of the velocities of horizontal movements of the surface

of the Earth's crust for the period 2017 – 2018 years
REFERENCES
1. Губин В.Н., Спутниковые технологии в геодинамике, Монография под ред. В. Н.

Губина. Минск: Минсктиппроект, 2010. 87 с, с. 3.
2. Етирмишли Г.Дж., Рзаев А.Г., Казымов И.Э., Казымовa C.Э. Моделирование
геодинамической ситуации Kуринской впадины на основе новейших сейсмоло-
гических, геодезических и магнитометрических данных, Бюллетень Оренбургского
научного центра УрЩ РАН, 2018,№2, c. 1-11
3. Кадиров Ф.А., Мамедов С.К., Сафаров Р.Т., Исследование современной
геодинамической ситуации и опасности землетрясений деформации земной коры
территории Азербайджана по 5-летним GPS- данным, Современные методы
обработки и интерпретации сейсмологических данных, Обнинск, 2015 г., с. 156-162
4. Казымов И.Э. Геодинамика Абшеронского полуострова, Современные методы
обработки и интерпретации сейсмологических данных, Обнинск, 2015 г., c. 163-166
5. Казымов И.Э., Казымова А.Ф. Современная геодинамика Азербайджана по данным
GPS станций за 2017-2018 гг., SEISMOPROGNOSIS OBSERVATIONS IN THE
TERRITORY OF AZERBAIJAN, Volume 16, № 1, 2019, c 35-42
6. Казымов И.Э., Рахимли З.С., Юзбашиева С.С. Общие принципы oбработки
спутниковых измерений сети GPS станций Азербайджана, Геофизический институт
Владикавказского научного центра РАН Геология и Геофизика Юга России,
№1/2017, Владикавказ 2017, ISSN 2221-3198, c 100-114
7. Robert E. Reilinger, Simon McClusky, Philippe Vernant, Shawn A. GPS constraints on
continental deformation in the Africa-Arabia-Eurasia continental collision zone and
implications for the dynamics of plate interactions: EASTERN MEDITERRANEAN
ACTIVE TECTONICS, journal of geophysical research vol. 111, 2006,
DOI:10.1029/2005jb004051
8. Yetirmishli G.J., Veliyev H.O., Kazimov I.E., Kazimova S.E. Correlation between GPS
observation outcomes and depth structure in studying horizontal movements, Бюллетень
Оренбургского научного центра УрЩ РАН, 2018,№4, p. 72-85
FOCAL PARAMETERS OF THE OGUZ EARTHQUAKE

SEPTEMBER 4, 2015 with ml = 5.9
S.E. Kazimova1, S.S. Ismayilova.1
Studying the conditions for the formation of the earthquake source is of great importance for
understanding the essence of seismic phenomena and developing methods for predicting seismic
hazard. In this case, the main parameters of the study are seismic waves. At the present stage, a
dense network of highly sensitive digital seismic stations, which allows recording all seismic events
with a magnitude of ml> 0.1 within Azerbaijan, as well as extensive factual materials obtained from
this network, have made it possible to develop many new methodological issues and outline new
ways of predicting earthquakes. The purpose of this article was to determine the dynamic
parameters of the source of a strong Oguz earthquake, as well as the solution of its mechanism.
On September 4, 2015, an earthquake with an observed intensity at the epicenter of I0 = 7
points and I0 = 7-3 points in nearby areas occurred near Oguz district. In accordance with the map
of epicenters of seismic events for 1900-2003 in the region of the earthquake that occurred, a
number of strong earthquakes were noted, with intensity at the epicenter of 6 or more points (Fig.1).
The most significant of them are the earthquakes of 1953, 1968 with I0 = 6-7 points, 1980, 1986,
1991 with I0 = 5-6 points, March 5, 2000 I0 = 5 points. The last tangible seismic event in this area
was an earthquake on June 1, 2003 with I0 = 6 points in the epicenter and 3-4 points in the regions
of Mingachevir and Kurdamir (table 1) [1, 2].
Figure 1. Map of the epicenters of strong earthquakes in the study area for the period 1900-2003.
1
Table 1. Strong earthquakes in Oguz and surrounding areas with an intensity

at the epicenter of 5 or more points [1]
Date Time Coordinates Depth

northern eastern Io
MI
year month day hour min sec latitude longitude km points
degrees degrees
1953 9 2 00 36 01 41.10 47.40 5 5.1 7
1953 9 16 11 15 29 41.20 47.40 28 5.0 6
1968 5 11 11 29 40 41.00 47.60 15 4.7 6
1980 4 1 07 33 41 40.70 47.80 20 4.7 6
1986 6 02 15 16 13 40.97 47.77 22 4.6 5
1991 10 21 11 58 23 40.92 47.34 16 4.5 5
2003 06 01 06 09 42 41.05 47.27 22 5.0 6
Instrumental data
Seismic vibrations from the September 4, 2015 earthquake were recorded by 18 world
agencies and nearly 400 seismic stations in a wide azimuthal environment at distances from 300 to
13,407 km from the epicenter. The main parameters of the earthquake obtained by the Republican
Seismic Survey Center of Azerbaijan are represented in Table 1. Based on macroseismic studies, it
was revealed that the earthquake was felt most intensely in the Oguz and Sheki regions. Here, the
intensity of the earthquake according to MSK-64 scale was estimated at 7 points. The earthquake
was accompanied by more than 80 aftershocks with magnitudes from 0.5 to 4, 33 of which occurred
on the first day [3,4]. The aftershock cloud spread up to 23 km in the direction of the south-west
and 9 km in the direction of the west-east, however, the area of the main mass of the earthquake
accumulation was 88 km2. Despite
the fact that the main source is
located at a depth of 16 km in the
granite layer, the depth of aftershocks
varies between 11-34 km. As seen in
Fig.2 the earthquake epicenter is
confined to the zone of intersection of
the longitudinal Dashgil-Mudrese and
transverse Arpa-Samur faults [5]. It
should be noted that the Arpa-Samur
deep fault of the ancient formation at
all times from the Paleozoic to the
present day is a zone of active
manifestation of tectonic movements,
a conductor of magmatic melts, ore-
bearing solutions and seismicity.
According to Shikhalibeyli E.Sh. [6]
the Arpa-Samur trans-Caucasian
seismic-metal-bearing fault zone
combines the Mrovdag-Zodsky,
Terter and Khachinsky deep faults.
Figure 2. Aftershock field of the strong Oguz earthquake on

September 4, 2015 with ml = 5.9
Faults: I - Arpa-Samur, II - North Adzhinour, III - Vandam,
IV - Dashgil-Mudrese [4]
S.E. Kazimova, S.S. Ismayilova: FOCAL PARAMETERS OF THE OGUZ EARTHQUAKE… 25
The solution of the source mechanism

The focal mechanism solution was obtained by the method of waveform inversion - Time-
Domain Moment Tensor INVerseCode (TDMT INVC), developed by Doug Draeger from the
University of California, Berkeley [7]. This package is used to calculate both the seismic moment
tensor and Mw. In this method, the seismic moment tensor is determined on the basis of the
inversion of the low-frequency part of the broadband 3-component waveform and then decomposed
into the scalar seismic moment Mo and the orientation parameters of the strike, slip and rake forces.
The moment magnitude Mw of interest to us is determined from the scalar seismic moment
according to Kanamori [8]:
Mw = [log 10 (Mo) - 16.1] / 1.5
The main source of RSSC ANAS seismograms. There is also information about the
hypocenter and time at the source of the earthquake. Seismograms are downloaded in SEED format
and converted to SAC format (Fig. 3). Broadband seismograms are selected subject to a distance
limit (50-350 km). They should have a sufficient duration (the interval from P-waves to the initial
part of S-waves is included) and quality (sufficiently high signal-to-noise ratio, lack of clipping).
Preparation of seismograms for inversion includes: removal of the entry of the P-wave;
deconvolution (restoration of true soil displacements); determination of epicenter distance, direct
and reverse azimuths; calculation of radial and transverse components; filtering. Deconvolution
takes place in the time domain [8]. For bandpass filtering, a 4-order Butterworth filter is used. If
necessary, decimation is carried out in order to make the sampling frequency equal to 1 count per
second. That is, lead to the same time step that the influence functions have: 1 second. In addition,
the time interval that is used to solve the problem is determined.
Figure 3. Wave recording of the Oguz earthquake in SAC format
Thus, the mechanisms of two earthquakes were constructed and analyzed: September 4, 2015
with ml = 5.9 (main shock) and October 13, 2015 with ml = 4.0. An analysis of the mechanisms of
the sources of these earthquakes showed the predominance of two types of movements. The
earthquakes that occurred in the Oguz region on September 4 at 04h 49m and October 13 at 00h 13m
occurred under the action of tensile and compressive stresses of similar magnitude. Table 2 shows
that the first nodal plane of the gap extends in the SE direction (153º) with a fall to the south-west at
an angle of 86-90º, the second nodal plane has a NE strike (63º) with a fall to the south-east at an
angle of 83-90º. In this case, the compressive stresses in the earthquake source were oriented in the
north-east direction (azimuth 18) and acted near horizontally (angle with the horizon 0-7), and
tensile forces were directed in the west-south-west direction (287-288) at an angle of 0-2 to the
horizon. The type of movement of these earthquakes is a shift with a left-side horizontal
component.
Table 2. Parameters of the mechanisms of the Oguz earthquake’s sources in 2016 with ml = 5.9-4.0
Figure 4. Earthquake source mechanisms, as well as block diagrams of displacement along the NP2 plane
The epicenters of the Oguz earthquakes are confined to the Arpa-Samur fault and can be
interpreted as left-side shift deformation in the zone of geodynamic influence of the left-sided Arpa-
Samur fault. Figure 4 shows the stereograms of the mechanisms of the sources of the two analyzed
earthquakes, as well as the block diagram of the displacement along the NP2 plane corresponding to
the specified fault. Figure 5 shows how aftershocks migrate north-eastward along the transverse
fault, deepening to a depth of 35 km. It should be noted that the analysis of the mechanisms of the
other two aftershocks (2015.09.04 with ml = 3.3 and 2015.09.29 with ml = 3.3) showed the fault
type of underthrusts, which is associated with the influence of the North Adzhinour strike
longitudinal fault.
Figure 5. Three-dimensional model of the aftershock field of the Oguz earthquake on September 4, 2015 with ml = 5.9
Faults: I - Arpa-Samur, II - North-Adzhinour
It was said above that the earthquake data were recorded by 18 world agencies. A
comparative analysis of the results of solutions of the focal mechanism in different regions was
carried out. It was found that the solution of the seismic moment tensor of the centroid USGS and
GFZ is close to the solution obtained from the RSSC seismic station network (Fig. 6).
Figure 6. Focal mechanisms of Oguz earthquakes according to USGS and GFZ
Dynamic parameters.
Using the digital seismograms of the transverse waves of earthquakes, the Fourier amplitude
spectra were constructed, which made it possible to determine the maximum level of the spectrum
and the boundary upper frequency of the maximum level f0. In the calculations, the classical model
of D.Brun [9] was used. To determine the dynamic parameters of the earthquake sources, only S-
wave recordings were used at 8 digital stations: Zagatala, Khinalig, Siyazan, Sheki, Saatly, Guba,
Gusar and Pirkuli (Fig.7). To determine the parameters of the spectrum, it is approximated by two
straight lines - a straight line parallel to the frequency axis (horizontal strike), in the low-frequency
region and an inclined straight line in the high-frequency region. The interval of epicenter distances
for the stations under consideration turned out to be Δ = 30-200 km.
“ZKT” HGE “XNQ” HGE

1.0E+08 1.0E+08
1.0E+07 1.0E+07
1.0E+06 1.0E+06
1.0E+05 1.0E+05
1.0E+04 1.0E+04
A(count)
A(count)
1.0E+03 1.0E+03
1.0E+02 1.0E+02
1.0E+01 1.0E+01
1.0E+00 1.0E+00
1.0E-01 1.0E-01
1.0E-02 1.0E-02
0.1 1.0 10.0 100.0 0.1 1.0 10.0 100.0
f(Hz) f(Hz)
“SIZ” HGE “SEK” HGE

1.0E+08 1.0E+08
1.0E+07 1.0E+07
1.0E+06 1.0E+06
1.0E+05 1.0E+05
1.0E+04 1.0E+04
A(count)
A(count)
1.0E+03 1.0E+03
1.0E+02 1.0E+02
1.0E+01 1.0E+01
1.0E+00 1.0E+00
1.0E-01 1.0E-01
1.0E-02
1.0E-02
0.1 1.0 10.0 100.0 0.1 1.0 10.0 100.0
f(Hz) f(Hz)
“SAT” HGE “QUB” HGE

1.0E+08 1.0E+08
1.0E+07 1.0E+07
1.0E+06 1.0E+06
1.0E+05 1.0E+05
1.0E+04 1.0E+04
A(count)
A(count)
1.0E+03 1.0E+03
1.0E+02 1.0E+02
1.0E+01 1.0E+01
1.0E+00 1.0E+00
1.0E-01 1.0E-01
1.0E-02 1.0E-02
0.1 1.0 10.0 100.0 0.1 1.0 10.0 100.0
f(Hz) f(Hz)
“QSR” HGE “PQL” HGE

1.0E+08 1.0E+08
1.0E+07 1.0E+07
1.0E+06 1.0E+06
1.0E+05 1.0E+05
1.0E+04 1.0E+04
A(count)
A(count)
1.0E+03 1.0E+03
1.0E+02 1.0E+02
1.0E+01
1.0E+01
1.0E+00
1.0E+00
1.0E-01
1.0E-01
1.0E-02
1.0E-02
0.1 1.0 10.0 100.0
0.1 1.0 10.0 100.0
f(Hz) f(Hz)
Figure 7. Amplitude spectra of the Oguz earthquake on September 4, 2015
The following spectral characteristics were determined: the angular frequency f0, the radius of
the circular dislocation r0, the discharged tension , the source volume V, the average
displacement along the discontinuity D. Table 3 also presents the values of the moment magnitude
Mw and seismic moment M0 calculated earlier using the tensor method seismic moment based on
the inversion of the low-frequency part of the broadband 3-component waveform [7].
The values of the released tension appear to be underestimated. This is due to the fact that
the radius of a circular dislocation can vary from station to station, depending on the position
relative to the discontinuity plane and the direction of movement in the focus. This analysis
showed the possibility of estimating dynamic parameters from observations of one station in a
wide frequency range. Thus, the focal parameters of the Oguz earthquake are as follows:
angular frequency f 0 = 1.0 Hz, seismic moment M 0 = 2.6 * 1024, dyn ∙ cm, circular dislocation
radius r0 = 1.4 km, released tension  = 44 dyn/cm 2, source volume V = 12 km 3, average
displacement along the fault D = 1.03 * 10-2 m.
Table 3. Dynamic parameters of the Oguz earthquake of September 4, 2016 with ml = 5.9
№ Ω0, сm∙с2 F0, Hz M0,1024, dyn-cm Mw R0, km Δσ, dyn/сm2 D,10-2, m V, km3
1 2 3 4 5 6 7 8 9
1 ZKT 1.1 2.6 5.5 1.25 55.81 1.23 8.2
2 XNQ 1.0 2.6 5.5 1.38 41.93 1.02 11.0
3 SIZ 1.0 2.6 5.5 1.38 41.93 1.02 11.0
4 SEK 1.2 2.6 5.5 1.15 72.46 1.47 6.4
5 SAT 0.9 2.6 5.5 1.53 30.57 0.83 15.0
6 QUB 0.8 2.6 5.5 1.72 21.47 0.65 21.4
7 QSR 0.9 2.6 5.5 1.53 30.57 0.83 15.0
8 PQL 1.1 2.6 5.5 1.25 55.81 1.23 8.2
Average value 1.0 2.6 5.5 1.4 44 1.03 12
It is known that the nature of the movements recorded on the seismogram is determined both
by the medium along the seismic wave propagation path and by the source, a comprehensive
analysis of the record is required, which would allow obtaining additional information about the
earthquake source, and better understand the source mechanism [10].
An important point in the calculation of dynamic parameters is the transition from the station
spectrum to the focal spectrum. For such a transition, it is necessary to take into account the influence
of the medium (“attenuation”) and the amplification factor on the path of the seismic beam. There are
various methods for determining station corrections, which are described in works [11–13]. The
purpose of the research is the calculation of station corrections (determination of the site effect of the
station) based on the analysis of the seismic signal using the Nakamura method [14].
Calculation methodology
As is known, displacements of the earth's crust are measured in three directions: north-south
(NS), east-west (EW) and vertically (Z). Nakamura's method is to find the ratio of the spectrum of
the horizontal component (H) to the spectrum of the vertical (V). For this, it is necessary to use
measurements of the 3 components of the E, N, Z seismogram [14]. The calculation of the
component H occurs as the quadratic mean of the spectra of the E and N components, vertical V
corresponds to the spectrum of the component Z. Next, the H / V ratio is directly calculated:
Thus, we analyzed the data of digital records of the transverse wave for the three components
HGE, HGN, HGZ of 21 stations of the main shock. In the study, the duration of the recording time
window was 60 seconds.
A linear trend is eliminated from the selected recording section and, to prevent spectrum
leakage, the signal is smoothed at the ends using a 5% cosine window. Corrections for the
measurement error of the instrument are applied to the resulting series and the spectrum is
calculated using the Fourier transform [12].
Thus, the spectral ratios were calculated and the amplification factor of 21 broadband digital
earthquake stations that occurred on September 4, 2015 in the Oguz region with a magnitude of 5.9
was found (Fig. 8, 9, 10). We divided the result into three classes: stations for which the maximum
values of the extension factor fluctuate in the frequency range 0.2-1.0 Hz (stations "ALI", "GBS",
"GLB", "LKR", "PQL", "QBL", “QSR”, “XNQ”, “ZKT”,), stations for which the maximum values of
the extension factor fluctuate in the frequency range 1.0-4.0 Hz (stations “ATG”, “HYR”, “IML”
“MNG”, “QUB” , “SIZ”), and in the range 3.0–7.0 Hz (stations AST, GAN, LRK, ORB, SEK, BRD).
Figure 8. The seismic wave amplification factor at the stations “ALI”, “GBS”, “GLB”,
“LKR”, “PQL”, “QBL”, “QSR”, “XNQ”, “ZKT”.
Figure 9. Seismic wave amplification factor at “ATG”, “HYR”, “IML”, “MNG”, “QUB”, “SIZ” stations
Figure 10. Seismic wave amplification factor at the stations “AST”, “GAN”, “LRK”, “ORB”, “SEK”, “BRD”
This method is based on the notion that the influence of a thin layer (a small layer of the
earth’s crust immediately below the seismic station) of the object under study mainly refers to
transverse waves (S-wave), which are amplified by this structure and practically do not change
longitudinal waves (P -wave). Then the ratio of the spectral characteristics of two horizontal
components to the spectrum of the vertical component will characterize the so-called transfer
function, which strictly depends on the thin layer under the study object [12]. It was found that the
maximum extension factor is characteristic for the stations “QBL” = 3.6, “AST” = 4.3, “GAN” =
4.3, “SEK” = 3.6, “BRD” = 3.4.
Conclusions
Thus, despite the fact that the main source of the Oguz earthquake that occurred on September
4, 2015, 04h 49m with ml = 5.9, was located at a depth of 16 km in the granite layer, the depth of
aftershocks varies between 11-34 km. The aftershock cloud spread up to 23 km in the direction of the
SW and 9 km in the direction of the WE, the area of the main earthquake accumulation was 88 km2.
Based on the solution of the source mechanism, it was found by the method of inversion of
wave forms that the earthquakes that occurred in the Oguz region on September 4 at 04h 49m and
October 13 at 00h 13m occurred under the action of tensile and compressive stresses of similar
magnitude. In this case, the compressive stresses in the earthquake source were oriented in the
north-east direction (azimuth 18) and acted horizontally (angle with the horizon 0-7), and tensile
forces were directed in the west-south-west direction (287-288) at an angle of 0-2 to the horizon.
The type of movement of these earthquakes is a shift with a left-side horizontal component. An
analysis of the mechanisms of the other two aftershocks (2015.09.04 with ml = 3.3 and 2015.09.29
with ml = 3.3) showed the fault type of movements. Earthquakes are confined to the zone of
intersection of the longitudinal Dashgil-Mudrese and transverse Arpa-Samur faults, which are the
zone of active manifestation of tectonic movements to this day.
Using the digital seismograms of the transverse waves of earthquakes, the Fourier amplitude
spectra were constructed, which made it possible to determine the maximum level of the spectrum
and the boundary upper frequency of the maximum level f0. The focal parameters of the Oguz
earthquake are as follows: angular frequency f0 = 1.0 Hz, seismic moment M0 = 2.6 * 1024, dyn ин
cm, circular dislocation radius r0 = 1.4 km, released tension  = 44 dyn / cm2, source volume V =
12 km3, average displacement shift D = 1.03 * 10-2 m. Based on the said above, the spectral ratios
were calculated and the gain factor of 21 broadband digital stations was found. It was found that the
maximum extension factor is characteristic for the stations “QBL” = 3.6, “AST” = 4.3, “GAN” =
4.3, “SEK” = 3.6, “BRD” = 3.4.
Summing up, it should be noted that further detailed and comprehensive study of the buried
Arpa-Samur trans-Caucasian seismically active seismic-metal-bearing fault zone of deep faults,
which has been active for a long time and sharply influenced the structure of the East Caucasus, can
provide ample material for understanding geodynamic processes in this part of Mediterranean belt
in the alpine cycle.
REFERENCES
1. Гасанов А.Г., Абдуллаева Р.Р., Азербайджан // Землетрясения Северной Евразии в

2003 г., Обнинск, 2009 г., с. 58-67.
2. Ахмедбейли Ф.С., Гасанов А.Г., Тектонические типы сейсмических очагов
Азербайджана, Баку 2004 г., с 60-61.
3. Yetirmişli Q.C., Abdullayeva R.R., İsmailova S.S., Kazımova S.S., 2015-ci ildə Azərbaycan
və ətraf bölgələrin seysmikliyinin xüsusiyyətləri // İllik Hesabat, 2015-ci il, s...
4. Yetirmişli Q.C., İsmailova S.S., 2015-ci ildə Azərbaycan ərazisində baş vermiş zəlzələlərin
kataloqu, Bakı, 2015-ci il.
5. Гасанов А.Г., Глубинное строение и сейсмичность Азербайджана в связи с прогнозом
нефтегазоносности, Баку: Элм, 2001 г., с. 166-187.
6. Шихалибейли Э.Ш. Некоторые проблемные вопросы геологического строения и
тектоники Азербайджана. Баку: Элм, 1996. 215с.
7. Dreger D.S., Time-Domain Moment Tensor INVerseCode (TDMT_INVC) // University of

California, Berkeley Seismological Laboratory, 2002. 18 р.
8. Hanks T.S., Kanamore H.A. A moment magnitude scale // J.Geophys. Res. – 1979. – 84.
№ 135. - Р.2348-2350. 25–33.
9. Brune J.N. Tectonic stress and the spectrum of seismic shear waves from earthquake //
J.Geophys. Res. – 1970. – 75. № 26.- Р.4997-5009.
10. Лемзиков В.К., Лемзиков М.В. Особенности затухания сейсмических волн в
вулканических средах Камчатки, Институт вулканологии и сейсмологии ДВО РАН,
Петропавловск-Камчатский. 176-185 с.
11. Bindi D., Parolai S., Spallarossa D., Catteneo M. Site effects by H/V ratio: Comparison of
two different procedures / D. Bindi, S. Parolai, D. Spallarossa, M. Catteneo // Journ. of
Earthquake Engin. 2000. Vol. 4. № 1. P. 97–113. 3.
12. Parolai S., et al. Comparison of Different Site Response Estimation Techniques Using
aftershocks of the 1999 Izmit Earthquake / S. Parolai, D. Bindi, M. Baumbach, H. Grosser,
C. Milkereit, S. Karakisa, S. Zunbul // Bulletin of the Seismological Society of Amer. June,
2004. Vol. 94. № 3. Р. 1096–1108. 2.
13. Picozzi M., et. al Site characterization by seismic noise in Istanbul, Turkey / M. Picozzi, A.
Strollo, P. Parolai, E. Durukal, O. Ozel, S. Karabulut, J. Zschau, M. Erdik // Soil Dynamics
and Earthquake Engineering. 2008. P. 2–6. 4.
14. Nakamura Y. A method for dynamic characteristics estimation of subsurface using
microtremor on the ground surface / Y. Nakamura // QR Railw. Tech. Res. Inst. 30.
1989. P. 25–33.
COMPARATIVE ANALYSIS OF GRAVIMETRIC STUDIES IN BOZDAG-GOBU MUD

VOLCANO AND SURROUNDING AREAS
E. M. Baghırov1, A. T. İsmayılova1
Carrying out frequent measurements of non-tidal variations of relative gravity force

according to relief in the area for construction of electric station in the Bozdagh-Gobu volcano and
adjacent areas have been implemented by the use of the GC-5 Autograv device (Fig.1) according to
17 profiles, which include120 observation points. The geological structure of the site, the location
of the tectonic faults, dimensions of the mass which may be dynamics of activity, depth of the faults
and contours of probable potential hazard zones are determined based on the information obtained
during the selection of gravimetric profiles. Additional frequent measurements have been carried
out with gravimetry method absolutely in the10 profiles that length up to 3 km from the main
construction site to volcanoes and in the volcano area in 3 and 5 profiles, in addition to covering the
ES and the substation area which to be built. The distance between the project profiles and
observation points are 100 meter and the researches have been done at each point taking 4
dimension value one in 60 seconds. The measurements are repeated with the condition of return to
the back/support point after the accomplishment of the measurements for the each profile.
Figure 1. The view of the CG-5 AutoGrav gravimetry produced by Canada which the research works carrying out
Gravimetric researches have been conducted in the Bozdagh-Gobu volcano and adjacent areas
on the designed profiles (Fig. 2.) and these researches have been implemented on the observation of
the emergency differences in the gravitational acceleration between the two points. This method
allows to improve the accuracy of the measurements and it is one of the leading methods for
detecting depth fault, gradient zones, displacement, deformation of the gravity force in the inner
structure of the earth. This enables us to evaluate the geological processes in the deeper layers of the
crust in the research area and it provides to analyze complexly the direct relationship between
geological processes and seismic activity.
The main purpose of the research is to study the fault-block structure of the Earth’s crust due
to non-tidal variations in the gravitational field for the construction works near the Bozdagh-Gobu
volcano and is the assesment of geodynamic condition during the formation of structures involving
a complex geophysical data in that area.
Observable values about the variation character according to time of the gravity force among
the observation points have been processed considering all of the adjustments.The following results
of the relative gravity force, the obtained results according to the all research field have been
described visually in the form of A map, three-dimensional model and transects (Fig.3-7).
1
Zones monitored with ∆g, profiles, observation points and the risk areas for have been clearly
covered by the isoanomal maps of the gravitational field construction (Fig. 3,8,9,10). Now, let’s try
to analyze the isoanomal maps of the gravitational field.
As shown in the isoanomal map (3. map) of the gravitational field, the anomalous zones have
been observed with the variable characteristic of the relative gravity force values have been
precisely covered. Composition of the rocks in the research field have been sharply differentiated
by their density. This is due to the fact that it has been covered by sand, clay sand,volcanic breccia
of mud volcano and etc.. The differentiation of such density take mosaic shaping of gravity force
propagation forward. However, a regularity is recorded in the map. Thus, the relative gravity force
(density of rocks) increases from the western part of the research areas to the eastern part from 11.5
mQal to 2.5 mQal.
Most porous rocks are in the western part of the field. It is clear that, the area which we are
investigate is not stable from the point of geology.Basically, there are anomalous zones and
sediment in the probable lower layer in the center of profiles III, IV, V.
Accordingly, 3D model of gravitational field (Fig. 4), transects on profiles according to
isoanomal maps (Fig.5),diagram (Fig.6) and graphs (Fig.7) have been created. It is clear that form
the transects on profiles, model diagram and graphs.
Gravimetric researches have been carried out in the area over the salt lake, up to the volcano
in ≈ 3 km distance on 3 profiles (Fig.8) and on 5 profiles (Fig. 9) on the volcano crater considering
the importance and expedient of studying the impact of the Bozdagh-Gobu volcano located in the
north-eastern part of “Gobu” substation area with 330/220/110 kV and
Gobu Electric Station with 385 MVt will be built in “Gobu” area after studying the main
research field.
Figure 2. Scheme of the research field

E. M. Baghırov, A. T. İsmayılova: COMPARATIVE ANALYSIS OF GRAVIMETRIC STUDIES IN BOZDAG-GOBU... 35
Observation Points
Unfavorable area Profiles
Figure 3. Isoanomal maps of the gravitational field.
Figure 4. 3D model of the gravitational field corresponding to the isoanomal maps

Observation points Observation points
Figure 5. Transects on profiles according to the isoanomal maps of the gravitatioal field.
Figure 6. Model diagram on profiles according to the isoanomal maps of gravitational field
Figure 7. Comparative graphs on profiles according to the isoanomal maps of gravitational field
Profiles from the research area to the volcano
Figure 8. Isoanomal map of gravitational field in the area from the main research field to the Bozdagh-Gobu volcano.
Profiles above the volcano
Figure 9. Isoanomal maps of the gravitational field in the Bozdagh-Gobu volcano
Full research area
Figure 10. Isoanomal maps of gravitational field, fully covering the research area
Relative gravity force increases –6---2,5 mQal from south to north in the north direction in the
area of Bozdagh-Gobu volcano,that is, concentrated in the north and porous rocks are spread in the
north-east direction (Fig. 8). The relative gravity force increasing 8.5-----3.5 mQal is different in the
Bozdagh-Gobu volcano (Fig. 9).Finally, the isoanomal maps of gravitational field over an area
covered by 17 profiles are added to the article (Fig. 10).
Conclusions
- Anomal zones with variable characteristic value of ∆g are highlighted in the isoanomal map
of gravitatonal field
- The gravity force is not stable in this site and there are propably sediment, anomalous zones
in the center of III, IV profiles
- 3D model of the gravitational field have been created on the basis of Transects on profiles,
graphs and isoanomal map. Relative gravity force on total field varies between 11,5 ----- 2.5
mQal.
- The impact of Bozdagh-Gobu volcano to the construction site is minimum and the gravity
force in this site varies between 8,5 --- 3,5 mQal.
- Unfavorable area is determined for construction in the main research area.
REFERENCES
1. Гасанов А.Г. 2001 г., стр. 279., Глубинное строение и сейсмичность Азербайджана.
Баку, изд.Элм.
2. Шванк О.А. Интерпретация гравитационных наблюдений. Люстих Е.Н.
Гостоптехиздат, 1947 г.
3. Буланже Ю.Д. 1978г., стр. 10-17., Изучение неприливных изменений ускорения
силы тяжести. Сб.научных трудов. Повторные гравиметрические наблюдения
Москва, изд. “Нефтегеофизики”,
4. Немцов Л. Д. 1967 г., стр.46-57., Методика и техника высокоточных
гравиметрических работ. Высокоточная гравиразведка, Москва, изд. “Недра”.
5. Белоусов В.В. 1975 г.,стр. 260. Основы геотектоники.Москва, изд. “Недра”.
6. Сорокин Л.В. 1953 г., стр 156. Гравиметрия и гравиметрическая разведка.
Гостоптехиздат,изд.-3-е.
7. Кузмин В. И. 1973 г., стр.18-62.,Гравиметрия. Москва, изд.“Недра”.
STUDY OF THE LOW VELOCITY ZONES IN THE TERRITORY OF GOBU REGION

(AN EXAMPLE OF THE GOBU POWER STATION)
E.S.Garaveliyev1, A.V. Aghazade1
The territory of Gobu is located in the south-western part of the Western-Absheron

anticlinorium and there are small mountain range in the east-west - north-south direction, here.
There are numerous cones of the mud volcanoes in the hills of this area. The absolute height of the
area varies between 120-160 meters and there is the tendency to gradual grounding in the south-
west direction.
Territory of “Gobu” Electric Station located approximetly 2.5-3 km from Gobu-Bozdagh
mud volcano and about 6 km from Guzdek-Bozdagh mud volcano is the research area. Although
mud mass erupting out of the both volcanoes are less likely to reach to the living area, the Gobu-
Bozdagh mud volcano generates the shakes always noticeable with dynamic activity and
seismological signs and it caused serious damage in nearby houses.
The above-mentioned are the indications of complex seismological conditions of the “Gobu”
Electric Station area and its dynamic activity.
This volcano erupted in 1827, then in 1974 and last time in 1999 year. When the volcano
erupted, the flame height was 400 meters, and the temperature was more than 1,000 degrees. At the
same time, 300,000 thousand cubic meters of volcanic mud have been erupted and spread around.
The central part of the volcano’s crater rose to 6-7 m height and many broken blocks have been
formed there during the last eruption of this volcano in 1999 year. As the result of this, the large
cracks that depth is 2 m up to Hokmeli region and approximetly 1200 m length have been formed.
In the area where the “Gobu” electric station considered to be built in Gobu region, part of the
transect up to 10.0 m depth consists of the sediments of Paleogene Koun floor (P2k) based on the
materials of previous geological and engineer-geological researches. These sediments involves to
surface in the research area and consist of clays in terms of lithology. There are sandstones, schists
and occasionally marl gasket in these sediments. The layer of soil-plant which thickness is 0.1-0.3
meters is observed above the sediment of the Koun floor.
As mentioned above, the Gobu area is an area characterized by complex geological features.
Therefore, the research of small velocity zones during the construction-designing works in these
areas is very important. For the purpose of research a small velocity zone of this area, the “Broken
Microtremor” (Broken Microseisms) method of seismic exploration have been used (Loui, 2001).
This method is considered to be a profitable seismic method to establish a wide wave profile in the
research area in terms of substance and finance. Conducting such research will provide useful
seismic data in the areas of noisy urbanization.The phase data of wave area mentioned in the
“Broken Microtremor” (broken microseisms) is used.
The GEODE-24 engineering-seismic station, 24 seismic receiver for record the signals,
seismic exploration wire with115meter and hammer with 11 kg have been used for the purpose of
research of broken microseisms. Seismic source is the microshakes created by noise from the
environment and shake method.
In the area where the substation to be built,18 seismic profiles have been established
(preliminary materials of profile № 15 were unsatisfactory) and total amount of done works are
1955 linear meter.
Based on the obtained materials, there is a tectonic disturbance in the south of the “Gobu”
Electric Station with 385 MVt to be built in Gobu district (I.A. Israfilbeyov and V.A.Listerengarten.
Hydrological and Engineering Geology methods in the Absheron peninsula. Album of the
Hydrogeological and Engineering Geological Map of the Absheron Peninsula М 1: 50000, General
Directorate of Geodesy and Cartography of the Council of Ministers of the USSR, M .: 1983, s. 23-70).
1
E.S.Garaveliyev, A.V. Aghazade: STUDY OF THE LOW VELOCITY ZONES IN THE TERRITORY OF GOBU... 41
Figure 1. Relief changes in the western-Sonali residental area from the Gobu-Bozdagh volcano
Figure 2. The crater of the Gobu-Bozdagh volcano

Figure 3. Geometric dimensions of the research area (250 x250 m) and the location scheme of the seismic profiles in the site
Figure 4. Engineering geology map of the area (authors: İ.A.İsraphilbeyov and V.A.Listengarten).
Figure 5. Geological transect and slope of the layers in the north-eastern, edge part of the field (shell, sandy clay rocks).
Figure 6. Damage caused by volcanic eruptions on a farm near the foot of the Gobu-Bozdagh volcano.
Figure 7. During the field work.
As a result of initial visual observation, it is determined that the one part of the research was
inconvenient (sedimentary) from the point of view of construction (26000 m2 area).
Layers with the low wave speed (235-586 m/s) have been identified at a depth of about 6.5-
12.0 m from the surface and respectively 28-78.5 m. at depths in the transect of the 1; 4-7; 9-11; 13;
17 and 18 numbered profiles (these values are lower than others in the 1-8, 13, 16 and 18 numbered
profiles).
Layers with lower wave velocities are known to be unfavorable ground from a seismic point
of view. In this regard, it is important to implement additional engineer researches in the area.
Figure 8. Two-dimensional velocity sectiont (m / s) of transverse waves on the seismic profile No. 1.
Figure 9. Two-dimensional velocity section (m / s) of transverse waves on the seismic profile No. 2.
Conclusions
- Fuzzy slope of the layers in the small velocities zones investigated to a depth of 100 m in the
area, having the pinching out, the variation of the valuesof transverse seismic wave
velocities between 120-800 m/sec in the layers.
- It is identified that the grounds in the approximetly 6.5-12.0 m depths are very weak (empty,
soft or aqueous) and the unfavorable in terms of seismicity, starting from the surface on the
seismic profiles No. 1; 4-7; 9-11; 13; 17 and18 and laying of the unfavorable grounds are to
the depth of 3.0 m below the surface in the other 6 seismic profiles (with the exception of
No. 15)
- Low seismic velocities in all seismic profiles have been determined (at depths of 28-78.5 m,
with the wave velocities of 235-586 m / s). These values are lower than others on profile of
1-8, 13, 16 and 18 (235 -485 m/s).
- An unfavorable and sedimentary area for construction works has been identified in the
relief, south of the research area (100 m x 260 m= 26000 m2 in the area). There are
unevennesses with the amplitude up to 1.0 m. within this unfavorable area and the same
time, the color of the flora is completely different from the surrounding area.
REFERENCES
1. Balakişibəyli Ş.A., Qaravəliyev E.S. Sınan mikroseysmlər üsulunu tətbiq etməklə seysmik
kəşfiyyat işləri. Azərbaycan ərazisində seysmoproqnoz müşahidələr. Bakı; Nafta-Press,
2012, s. 39-45.
2. И.А.Исрафилбеков и В.А.Листенгартен. Гидрогеологические и инженерно-
геологические условия Апшеронского полуострова. Альбом гидрогеологических и
инженерно-геологических карт Апшеронского полуострова. М 1:50000, Главное
управление геодезии и картографии при Совете Министров СССР, М.: 1983, s. 23-70).
3. Louie, J, N., 2001, Faster, Better: Shear-wave velocity to 100 meters depth from refraction
microtremor arrays: Bulletin of the Seismological Society of America, v. 91, p. 347-364.
4. McMechan, G. A., and Yedlin, M. J., 1981, Analysis of dispersive waves by wave field
transformation: Geophysics, v. 46, p. 869-874.
5. Park, C. B., Miller, R. D. and Xia, J., 1998, Imaging dispersion curves of surface waves on
multi-channel record: Annual Meeting Abstracts, Society of Exploration Geophysicists,
1377-1380.
ANNOTATIONS
1. ASSESSMENT OF SEISMIC HAZARD IN THE TERRITORY OF

“TAKHTAKORPU” RESERVOIR OF AZERBAIJAN
G.J. Yetirmishli, T.Y. Mammadli, R.B. Muradov, T.I. Jaferov
Seismological researches were conducted at the Takhtakorpu reservoir built in the territory of
Shabran district. On the basis of earthquake data, active tectonic faults or potential source zones in
Shabran district and adjacent areas have been identified and their seismic potential has been
assessed. It was revealed that, the maximum magnitude of the probable earthquakes in the zone of
two large-sized active faults or potential source in the area close to the research area is M max = 7.4
and Mmax = 6.7, respectively. Seismic hazards may occur in conducted researches of the maximum
magnitude earthquakes in this source zones. The earthquakes with maximum magnitude in this
source zones can cause seismic hazards with an intensity of 8-9 points on the MSK-64 scale in the
territory of “Takhtakorpu” reservoir where researches were conducted.
Keywords: earthquake, active tectonic fault, source zones, seismic potential, magnitude,
seismic section.
2. ANOMALOUS CHANGES OF MAGNETIC FIELD BEFORE

THE ZAGATALA EARTHQUAKE ON 05.06.2018
A.G. Rzayev, L.A. Ibrahimova, N.B. Khanbabayev, M.K. Mammadova, V.R. Huseynova
Annotation: The formation character of the seismomagnetic effect have been studied before
the Zagatala earthquake (ml = 5.5; 05.06.2018) which was felt in the zones with high geodynamic
activity. About the non-homogeneous distribution of the local geomagnetic field tension in the
Shamakhi-Sheki-Balakan geodynamic polygon is provided.
Keywords: RSSC- Republican Seismic Survey Center, SME- seismomagnetic effect, nTI-nano
Tesla.
3. 1D VELOCITY MODEL BY LOCAL EARTHQUAKE DATA

S.E. Kazimova, Sh.N. Khadiji, S.E. Gummatli
The Caucasus-Caspian region is an area of complex tectonic structure accompanied by large

variations in seismic wave velocities and attenuation. In such areas, accurate geophysical models
are fundamentally important to seismic monitoring for two reasons: improved event location and
path calibration (critical for accurate estimation of event size and mechanism). In particular, the
great thickness and irregular geometry of the low velocity and low density sediments in the Kura
and Caspian sea basins causes profound effects on seismic waveforms, especially on surface waves
and regional phases. These effects are compounded by variation in crustal structure in the Caucasus
and by high attenuation under the e. Anatolian plateau [3].
Keywords: wave velocity, velocity model, hypocenter, earthquake, Velest.
4. ASSESSMENT OF MODERN GEODYNAMICS OF AZERBAIJAN

BY GPS MEASUREMENT DATA
G.J. Yetirmishli., I.E. Kazimov, A.F. Kazimova
The article presents the methodology for calculating the velocity fields of modern horizontal
displacements of the tectonic blocks in Azerbaijan, obtained from observations at 24 stationary GPS
RSSC stations, a characteristic aspect of which is a noticeable horizontal displacement in the north-
ANNOTATIONS 49
east direction at a speed of 5-18 mm / year. The velocities of joint seismic movement associated
with earthquake events were investigated using the GAMIT kinematic positioning program for 2017
and 2018 years. Maps of horizontal velocities were built according to the data of the geodetic
network of GPS stations of Azerbaijan for 2017 and 2018 years. An analysis of the data showed that
the distribution of the velocities of horizontal displacements to the north and east is not constant,
and the processes of shortening the surface of the Earth's crust in the study region are also not
constant.
Keywords: GPS stations, geodynamics, velocity fields of horizontal displacements, plate
tectonics.
5. FOCAL PARAMETERS OF THE OGUZ EARTHQUAKE

SEPTEMBER 4, 2015 with ml = 5.9
S.E. Kazimova, S.S. Ismayilova
The article analyzes a strong 7-magnitude earthquake that occurred on September 4, 2015, at
04h 49m in the Oguz region. The epicentral field, as well as the distribution of sources in depth,
was studied, and solutions to the mechanisms of the sources of the main shock and the most
noticeable aftershock were constructed and analyzed. The epicenters of the Oguz earthquakes are
confined to the Arpa-Samur fault and can be interpreted as left-side shift deformation in the zone of
geodynamic influence of the left-sided Arpa-Samur fault. A three-dimensional model of the
aftershock field is constructed. The Fourier amplitude spectra were constructed from digital
seismograms of the transverse waves of earthquakes, which made it possible to determine such
dynamic parameters as the angular frequency f0, seismic moment M0, the radius of the circular
dislocation R, the discharged stress, and the average underthrust along the structure D. Based on
the above said, The spectral ratios were calculated and an extension factor was found for 21
broadband digital stations.
Keywords: earthquake source, seismic moment, angular frequency, Fourier spectrum.
6. COMPARATIVE ANALYSIS OF GRAVIMETRIC STUDIES IN BOZDAG-GOBU

MUD VOLCANO AND SURROUNDING AREAS
E. M. Baghırov, A.T. İsmayılova
Assessment of the geodynamic conditions and study of the fault-block structure of the
consolidated crust due to insufficient variations in the gravitational field for the construction in the
area adjacent to the Bozdagh-Gobu volcano.
Keywords: Bozdagh-Gobu volcano, gravity, non-tidal variations, gravimetric field
7. STUDY OF THE LOW VELOCITY ZONES IN THE TERRITORY OF GOBU

REGION (AN EXAMPLE OF THE GOBU POWER STATION)
E.S. Garaveliyev, A.V. Aghazade
Study of the low velocity zones is especially important during the construction-designing works. As the result,
the seismic features and parameters of the geological transect are determined in the research area. One of the researches
has been carried out on the example of the Gobu Power Station to be built in the Gobu area. The upper transect of the
surface to the depth of 100 m have been studied using the “Broken Microseisms” method of the seismic exploration
during the research works.
Keywords: Seismic exploration, “Broken microseisms” methods, transverse wave velocity, GEODE -24 seismic
stations.
ANNOTASIYALAR
1. AZƏRBAYCANIN "TAXTAKÖRPÜ" SU ANBARI ƏRAZISINDƏ SEYSMIK

TƏHLÜKƏNIN QIYMƏTLƏNDIRILMƏSI
Q.C. Yetirmişli, T.Y. Məmmədli, R.B. Muradov, T.İ. Cəfərov
Şabran rayonunda inşa olunmuş Taxtakörpü su anbarı ərazisində seysmoloji tədqiqatlar

aparılmışdır. Zəlzələ məlumatları əsasında Şabran rayonu və ona yaxın ərazilərdə aktiv tektonik
qırılma və ya potensial ocaq zonaları müəyyənləşdirilmiş və onların seysmik potensialı
qiymətləndirilmişdir. Məlum olmuşdur ki, tədqiqat sahəsinə yaxın ərazidə kifayət qədər böyük
ölçülü iki aktiv qırılma və ya potensial ocaq zonalasında ehtimal olunan zəlzələlərin maksimum
maqnitudu müvafiq olaraq Mmax =7,4 və Mmax =6,7 təşkil edir. Bu ocaq zonalarında maksimum
maqnitudlu zəlzələlər tədqiqat aparılan "Taxtakörpü" su anbarı ərazisində MSK-64 şkalası üzrə 8-9
bal intensivlikli seysmik təhlükə yarana bilər.
Açar sözlər: zəlzələ, aktiv tektonik qırılma, ocaq zonaları, seysmik potensial, maqnituda,
seysmoloji kəsiliş.
2. 05.06.2018-CI ILDƏ ZAQATALA ZƏLZƏSINDƏN ÖNCƏ MAQNIT SAHƏSININ

ANOMAL DƏYIŞMƏLƏRI
A.Q. Rzayev, L.A. İbrahimova, N.B. Xanbabayev, M.K. Məmmədova, V.R. Hüseynova.
Yüksək geodinamik aktivliyi olan zonalarda hiss olunan Zaqatala zəlzələsindən əvvəl (ml =
5.5; 05.06.2018) seysmomaqnit effektinin yaranma xarakteri öyrənilmişdir.
Şamaxı-Şəki-Balakən geodinamik poliqonunda lokal geomaqnit sahə gərginliyinin qeyri-
bircinsli paylanması haqqında məlumat verilir.
Açar sözlər: RSXM-Respublika Seysmoloji Xidmət Mərkəzi, SME-seysmomaqnit effekt, nTl-
nano Tesla.
3. YERLI ZƏLZƏLƏLƏRIN MƏLUMATLARI ƏSASINDA

BIR ÖLÇÜLÜ SÜRƏT MODELI
Kazımova S.E., Xədici Ş.N., Hümmətli S.E.
Qafqaz-Xəzər bölgəsi mürəkkəb tektonik quruluş zonası kimi xarakterizə olunan regiondur.
Həmin ərazi seysmik sürətlərin böyük dalğalanması və seysmik dalğaların kəskin sönməsi ilə
xarakterizə olunur. Belə ərazilərdə dəqiq geofiziki modellər iki səbəbə görə prinsipial əhəmiyyət
daşıyır: zəlzələ ocaqlarının dəqiq koordinatların alınması və kolibrovkası üçün (mənbənin ölçüsünü
və mexanizmini dəqiq qiymətləndirmək üçün vacibdir). Xüsusilə Kür və Xəzər hövzələrində
çöküntü layın böyük qalınlığı və quruluşların nizamsız geometriyası aşağı sürətlər zonalar seysmik
dalğalara, xüsusən səth dalğalarına və regional fazalara güclü təsir göstərir. Bu təsirlər Qafqazdakı
yer qabığının quruluşunda dəyişiklik və Anadolu zonasında dalğaların yayılmasının tez sönməsi ilə
mürəkkəbləşir .
Açar sözlər: dalğaların sürəti, sürət modeli, hiposentr, zəlzələ, Velest proqramı
4. GPS MƏLUMATLARI ƏSASINDA AZƏRBAYCANIN MÜASIR

GEODINAMİKASININ GIYMƏTLƏNDIRILMƏSI
Q.C. Yetirmişli , İ. E. Kazımov , Kazımova A.F
Məqalədə 24 stasionar GPS_RSXM stansiyalarda aparılan müşahidələr nəticəsində əldə

edilən Azərbaycanın tektonik bloklarının müasir horizontal yerdəyişmələrinin sürət sahələrinin
hesablanması metodologiyası təqdim olunur. Xarakterik bir cəhət odur ki, şimal-şərq istiqamətində
ANNOTATIONS 51
5-18 mm sürətlə nəzərə çarpan horizontal yerdəyişməsidir. Tədqiqatlar 2017 və 2018-ci illər üçün
GAMIT proqramı üzərində aparılmışdır. Məlumatların təhlili göstərdi ki, horizontal yerdəyişmə
sürətlərinin şimal və şərqə paylanması daimi deyil və tədqiq olunan bölgədəki yer qabığının
səthinin qısaldılması prosesləri də həmçin dəyişir.
Açar sözlər: GPS stansiyaları, geodinamika, horizontal yerdəyişmələrin sürət sahələri,
plitələrin tektonikası
5. 4 SENTYABR 2015-CI IL TARIXINDƏ ML = 5.9 OLAN OGUZ

ZƏLZƏLƏSININ FOKAL PARAMETRLƏRI
S.E. Kazımova, S.S. Ismayılova
Məqalədə 4 sentyabr 2015-ci il tarixində, saat 04: 49-da Oğuz bölgəsində baş verən 7 bal gücündə
zəlzələ təhlil edilmişdir. Episentral sahə, habelə zəlzələlərin dərinliyə görə paylanması araşdırılmış və əsas
təkanın və ən çox hiss olunan afterşokların ocaq mexanizmləri qurulmuş və təhlil edilmişdir. Oğuz
zəlzələsinin episentrləri Arpa-Samur qırılması ilə uzlaşır və həmin qırılmanın təsiri altında sol tərəfli
horizontal yerdəyişmə gərginlik deformasiyə kimi xarakterizə olunur. Aftershock sahəsinin üçölçülü modeli
qurulmüşdur. Zəlzələlərin eninə dalğaların HG kanalların əsasında Furye spetktrları qurulmuş. Bu da bucaq
tezlikl f0 maksimal səviyyəsini, seysmik momenti Mо, dairəvi yer dəyişmənin radiusu R, boşalmış gərginlik
 və qırılma üzrə yerdəyişmənin qiyməti D müəyyən etməyə imkan verdi. Yuxarıda göstərilənlərə əsasən
21 rəqamsal stansiyaların dalğaların spektrlərinin nisbətləri hesablanmış, gücləndirmə faktoru tapılmışdır.
Açar sözləri: zəlzələ ocağı, seysmik Moment, bucaq tezliyi, Furye spektri.
6. BOZDAĞ-QOBU PALÇIQ VULKANI VƏ ƏTRAF ƏRAZİLƏRDƏ APARILAN

QRAVİMETRİK TƏDQİQATLARIN MÜQAYİSƏLİ TƏHLİLİ
E.M. Bağırov , A.T. İsmayılova
Bozdağ-Qobu vulkanına bitişik ərazidə tikinti işlərinin aparılması üçün qravitasiya sahəsinin
qabarmayan variasiyalarına görə konsolidə olunmuş qabığın qırılma-blok quruluşunun öyrənilməsi
və geodinamik şəraitin qiymətləndirilməsi.
Açar sözlər: Bozdağ-Qobu vulkanı, ağırlıq qüvvəsi, qabarmayan variasiyalar, qravimetrik
sahə.
7. QOBU ƏRAZISINDƏ KIÇIK SÜRƏTLƏR ZONASININ TƏDQIQI (“QOBU”

ELEKTRIK STANSIYASI ƏRAZISININ TIMSALINDA
E.S.Qaravəliyev, A.V. Ağazadə
Tikinti-layihələndirmə işləri zamanı ərazilərin kiçik sürətlər zonasının tədqiqi xüsusi

əhəmiyyət daşıyır. Nəticə olaraq tədqiqat sahəsində geoloji kəsilişin seysmik xüsusiyyətləri və
parametrləri müəyyən edilir. Bu cür tədqiqatlardan biri Qobu ərazisində inşa ediləcək “Qobu”
Elektrik Stansiyası ərazisinin timsalında yerinə yetirilmişdir. Tədqiqat işləri zamanı Seysmik
kəşfiyyatın “Sınan Mikroseysmlər” üsulundan istifadə edərək yerin 100 m dərinliyə qədər üst
kəsilişi tədqiq edilmişdir.
Açar sözlər: Seysmik kəşfiyyat, “Sınan Mikroseysmlər” üsulu, eninə dalğa sürəti, GEODE-24
seysmik stansiyası
АННОТАЦИИ
1. ОЦЕНКА СЕЙСМИЧЕСКОЙ ОПАСНОСТИ ТЕРРИТОРИИ

ВОДОХРАНИЛИЩА “ТАХТАКЕРПЮ”, ПОСТРОЕННОГО В ШАБРАНСКОМ
РАЙОНЕ АЗЕРБАЙДЖАНА
Г.Дж. Етирмишли, Т.Я. Маммадли, Р.Б. Мурадов, Т.И. Джафаров
На территории резервуара Тахтакерпю, построенного в Шабранском районе, прове-

дены сейсмологические исследования. На основе данных о землетрясениях установлены
активные тектонические разломы или потенциальные очаговые зоны, определен их
сейсмический потенциал. Было установлено, что максимальная магнитуда вблизи
территории исследования, в достаточно крупных активных разломах или потенциальных
очаговых зонах составляет Mmax =7,4 и Mmax =6,7. Такие землетрясения с максимальной
магнитудой могут сотрясти территории резервуара Тахтакерпю с интенсивностью в 8-9
баллов по шкале MSK-64.
Ключевые слова: землетрясение, активный тектонический разрыв, очаговые зоны,
сейсмический потенциал, магнитуда, сейсмологический разрыв.
2. АНОМАЛЬНЫЕ ИЗМЕНЕНИЯ В МАГНИТНОМ ПОЛЕ ДО

ЗАКАТАЛЬСКОГО ЗЕМЛЕТРЯСЕНИЯ 05.06.2018
А.Г.Рзаев, Л.А. Ибрагимова, Н.Б. Ханбабаев, М.К. Маммадова, В.Р. Гусейнова
Изучен характер проявления сейсмомагнитного эффекта перед Загатальским ощути-

мым землетрясением (ml=5.5 05.06.2018) в зоне высокой геодинамической активности.
Показана неоднородность распределения локальной напряженности геомагнитного поля по
площади Шамахы-Шеки-Балакенского полигона.
Ключевые слова: РЦСС - Республиканский центр сейсмологической службы, сейсмо-
магнитный эффект, нТл - нано Тесла.
3. ОДНОМЕРНАЯ СКОРОСТНАЯ МОДЕЛЬ ПО ДАННЫМ МЕСТНЫХ

ЗЕМЛЕТРЯСЕНИЙ
С.Э. Казымова, Ш.Н. Хадиджи , С.Э. Гумматли
Кавказско-Каспийский регион представляет собой зону сложной тектонической

структуры, характеризующуюся большими колебаниями скоростей и резким затуханием
сейсмических волн. В таких областях для сейсмического мониторинга принципиально
важны точные геофизические модели по двум причинам: улучшение местоположения
сейсмического события и калибровка пути (критически важны для точной оценки размера и
механизма очага). В частности, большая толщина осадочного чехла и неправильная гео-
метрия структур с низкой скоростью и низкой плотностью в бассейнах Куры и Каспийского
моря оказывают сильное влияние на сейсмические волны, особенно на поверхностные волны
и региональные фазы. Эти эффекты усугубляются изменением структуры земной коры на
Кавказе и высоким затуханием в зоне Анатолийского плато.
Ключевые слова: скорость волны, скоростная модель, гипоцентр, землетрясение,
программа «Велест».
ANNOTATIONS 53
4. ОЦЕНКА СОВРЕМЕННОЙ ГЕОДИНАМИКИ АЗЕРБАЙДЖАНА ПО

ДАННЫМ GPS ИЗМЕРЕНИЙ
Г.Дж .Етирмишли, И.Э. Казымов, А.Ф. Казымова
В статье представлена методика расчета полей скоростей современных горизонтальных

смещений тектонических блоков Азербайджана, полученная по результатам наблюдений на
24 стационарных GPS РЦСС станциях, характерным аспектом, которого является заметное
горизонтальное смещение в северо-восточном направлении со скоростью 5–18 мм/год.
Исследования проведены на программе GAMIT за 2017 и 2018 гг. Анализ данных показал,
что распределение значений скоростей горизонтальных смещений на север и на восток не
постоянны, не постоянны также и процессы укорачивания поверхности земной коры в
регионе исследования.
Ключевые слова: GPS станции, геодинамика, поля скоростей горизонтальных
смещений, тектоника плит
5. ПАРАМЕТРЫ ОЧАГА ОГУЗСКОГО ЗЕМЛЕТРЯСЕНИЯ 4 СЕНТЯБРЯ 2015 Г.

С ML = 5.9
С.Э. Казымова, С.С. Исмайлова
В статье анализируется сильное 7-ми бальное землетрясение, произошедшее 4 сентября

2015 г., в 04h 49m в Огузском районе. Изучено эпицентральное поле, а также распределение
очагов по глубине, построены и проанализированы решения механизмов очагов основного
толчка и наиболее ощутимого афтершока. Эпицентры Огузских землетрясений приурочены к
Арпа-Самурскому разлому и могут быть проинтерпретированы как левосторонняя сдвиговая
деформация в зоне геодинамического влияния левостороннего Арпа-Самурского разлома.
Построена трехмерная модель афтершокового поля. По цифровым сейсмограммам попе-
речных волн землетрясений были построены амплитудные спектры Фурье, которые дали
возможность определения таких динамических параметров, как угловая частота f 0, сейс-
мический момент M0, радиус круговой дислокации R, сброшенное напряжение , средняя
подвижка по разрыву D. На основе выше сказанного были вычислены спектральные
отношения и найден фактор усиления для 21 широкополосных цифровых станций.
Ключевые слова: очаг землетрясения, сейсмический момент, угловая частота, спектр
Фурье.
6. ОСОБЕННОСТИ ГРАВИТАЦИОННОГО ПОЛЯ НА ВУЛКАНЕ ГОБУ-БОЗДАГ

И ПРИЛЕГАЮЩИХ К НЕМУ ОБЛАСТЕЙ
Е.М. Багиров, А.Т.Исмайлова
Изучения свойства блок разломов консолидированного слоя с помощью неприливных

вариаций гравитационного поля с целью введения строительных работ на прилагаемых
районах Гобу-Боздагского вулкана.
Ключевые слова: Гобу-Боздагский вулкан, гравитационное поле, неприливные вариации.
7. ИССЛЕДОВАНИЯ ЗОН МАЛЫХ СКОРОСТЕЙ НА ТЕРРИТОРИИ ГОБУ («НА

ПРИМЕРЕ ТЕРРИТОРИИ ЭЛЕКТРОСТАНЦИИ ГОБУ»).
Э.С.Гаравелиев, А.В.Агазаде
Исследования зон малых скоростей в районе проектно-строительных работ имеют

особое значение. Как результат были определены сейсмические особенности и параметры
геологического разреза в районе исследований. Одно из таких исследований было проведено
на примере территории электростанции Гобу, которая будет построена на территории Гобу.
Используя метод «Переломленные Микросейсмы» сейсморазведки был исследован разрез от
поверхности участка до 100 м глубины.
Ключевые слова: сейсморазведка, метод «Переломленные Микросейсмы», скорость
поперечных волн, сейсмостанция GEODE-24.
55
Scope of the Journal
The Journal "Seismoprognosis observations in the territory of Azerbaijan" is specializing on the

theoretical and practical aspects of seismology, engineering seismology and earthquake prediction. In the
journal are publishing scientific articles on seismology of local and foreign scientists.
The journal is officially registered by the Highest Certifying Commission under the President of
Azerbaijan Republic.
The journal publishes scholarly articles on seismology, historical seismicity, seismic source physics,
strong-motion studies, seismic hazard or risk, earthquake disaster mitigation and emergency planning,
engineering seismology, triggered and induced seismicity, volcano seismology, earthquake prediction,
geodynamics, GPS measurements, gravimetric, magnetic and electrometric investigations in seismogenic
areas.
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Works will only be considered if not previously published anywhere else and must not be under
consideration for publication in any other journal or book. Manuscripts must contain original work and
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56
CONTENTS
G.J. Yetirmishli, T.Y. Mammadli, R.B. Muradov, T.I. Jaferov: Assessment of seismic hazard
in the territory of “Takhtakorpu” reservoir of Azerbaijan………………….……………….......... 3
A.G.Rzayev, L.A. Ibrahimova, N.B. Khanbabayev, M.K. Mammadova, V.R. Huseynova:
Anomalous changes of magnetic field before the Zagatala earthquake on 05.06.2018………….. 8
S.E. Kazimova, Sh.N. Khadiji, S.E. Gummatl: 1D velocity model by local earthquake data…... 13
G.J.Yetirmishli, I.E. Kazimov, A.F.Kazimova : Assessment of modern geodynamics of
Azerbaijan by GPS measurement data…………………………………………………………… 18
S.E. Kazimova, S.S. Ismayilova: Focal parameters of the Oguz earthquake September 4, 2015
with ml = 5.9……………………………………………………………………………………... 23
E. M. Baghırov, A. T. İsmayılova: Comparative analysis of gravimetric studies in Bozdag-
Gobu mud volcano and surrounding areas……………………………………………………... 33
E.S.Garaveliyev, A.V. Aghazade: Study of the low velocity zones in the territory of Gobu
region (an example of the Gobu power station)………….………………………………………. 40
Annotations……………………………………………………………………………………… 48
______________________________
Volume 16, № 2, 2019

http://www.seismology.az/journal
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Editor of publishing house: Kh.M.Nabiyev
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ISSN 2219-6641

Volume 16, № 2, 2019

G.J.Yetirmishli (chief editor) A.G.Aronov (Belarus)

Responsible Secretary: Huseynova V.R.

ASSESSMENT OF SEISMIC HAZARD IN THE TERRITORY OF

G.J. Yetirmishli1, T.Y. Mammadli1, R.B. Muradov1, T.I. Jaferov1

– The Takhtakorpu reservoir

– active fault or potential source zones;

Figure 4. Location map of profiles I-I and II-II

Figure.5. Seismological transects by profiles

1. Новый каталог сильных землетрясений на территории СССР / Отв. редактор Н.В.

ANOMALOUS CHANGES OF MAGNETIC FIELD BEFORE

A.G.Rzayev1, L.A. Ibrahimova1, N.B. Khanbabayev1, M.K. Mammadova1, V.R. Huseynova1

Stm/st Ismayilli (May, June, July)

1D VELOCITY MODEL BY LOCAL EARTHQUAKE DATA

S.E. Kazimova1, Sh.N. Khadiji1, S.E. Gummatli1

COUPLED HYPOCENTER VELOCITY MODEL PROBLEM

1 Republican Seismic Survey Center of Azerbaijan National Academy of Sciences

BUILDING A 1D VELOCITY MODEL: DATA SELECTION AND INITIAL MODEL

Figure 1. Final 1D velocity models after 9 iterations by Velest program

Figure 2. Final schematic 1D velocity model

1. Гасанов А.Г., Глубинное строение и сейсмичность Азербайджана в связи с прогнозом

ASSESSMENT OF MODERN GEODYNAMICS OF AZERBAIJAN

G.J.Yetirmishli1, I.E. Kazimov1, A.F.Kazimova1

Figure 1a. Simplified topographic/bathymetric (SRTM30 PLUS; http://topex.ucsd.edu/WWW_html/

Azerbaijan's geodynamics assessment based on GPS measurements for 2017-2018 years

Figure 4. Comparative graph of the velocities of horizontal movements of the surface

1. Губин В.Н., Спутниковые технологии в геодинамике, Монография под ред. В. Н.

FOCAL PARAMETERS OF THE OGUZ EARTHQUAKE

S.E. Kazimova1, S.S. Ismayilova.1

Table 1. Strong earthquakes in Oguz and surrounding areas with an intensity

Date Time Coordinates Depth

Figure 2. Aftershock field of the strong Oguz earthquake on

The solution of the source mechanism

Mw = [log 10 (Mo) - 16.1] / 1.5

Figure 3. Wave recording of the Oguz earthquake in SAC format

Figure 6. Focal mechanisms of Oguz earthquakes according to USGS and GFZ

“ZKT” HGE “XNQ” HGE

“SIZ” HGE “SEK” HGE

“SAT” HGE “QUB” HGE

“QSR” HGE “PQL” HGE

Figure 7. Amplitude spectra of the Oguz earthquake on September 4, 2015

1. Гасанов А.Г., Абдуллаева Р.Р., Азербайджан // Землетрясения Северной Евразии в

7. Dreger D.S., Time-Domain Moment Tensor INVerseCode (TDMT_INVC) // University of

COMPARATIVE ANALYSIS OF GRAVIMETRIC STUDIES IN BOZDAG-GOBU MUD

Carrying out frequent measurements of non-tidal variations of relative gravity force

Figure 2. Scheme of the research field

Figure 3. Isoanomal maps of the gravitational field.

Figure 4. 3D model of the gravitational field corresponding to the isoanomal maps

Observation points Observation points

Observation points Observation points

Observation points Observation points

Profiles from the research area to the volcano

Profiles above the volcano

Figure 9. Isoanomal maps of the gravitational field in the Bozdagh-Gobu volcano

Full research area

STUDY OF THE LOW VELOCITY ZONES IN THE TERRITORY OF GOBU REGION

E.S.Garaveliyev1, A.V. Aghazade1

The territory of Gobu is located in the south-western part of the Western-Absheron