General evaluation on the seismicity of Turkey and Japan.
VISITING RESEARCHER 2019A, TERM OF AUGUST 26- NOVEMBER 21, 2019

Ozgur Tuna OZMENGeophysical Engineer
Ministry of Interior
Disaster and Emergency Management Presidency
Republic of Turkey

DISCLAIMER
Contents of this research paper is prepared by Mr. Ozgur Tuna OZMEN, Visiting Researcher of 2019 term
(August-November) Batch A, for the Asian Disaster Reduction Center, Kobe, japan.
This report was compiled by an ADRC visiting researcher (VR) from ADRC member countries. The views
expressed in the report do not necessarily reflect the views of the ADRC. The boundaries and names
shown and the designations used on the maps in the report also do not imply official endorsement or
acceptance by the ADRC.

CONTENTS
ACRONYMSACKNOWLEDGEMENTS
Chapter 1oIntroduction

06oRisk Profile of Turkey

08

Chapter 2oRecent Major Earthquakes in Turkey

11oNational Strong-Motion Network of Turkey (TR-NSMN)

26

oLocal Networks

30

Chapter 3oRecent Major Earthquakes in Japan

32

oStrong Earthquake Motion Observation in Japan38

The Japan Meteorological Agency (JMA) Seismic Intensity Network

38

K-Net and Kik-net

40

Seismic Intensity Information Network of Local Governments

40

Other National Research Institutes and Public Bodies

41

Public Works Research Institute, Ministry of Construction

41

Port and Harbour Research Institute, Ministry of Transport

42

Earthquake Research Institute (ERI), University of Tokyo

42

Tokyo Gas Co. Ltd.

42

Yokohama City

43

Building Research Institute (BRI)43

Nationwide Strong Motion Network of BRI

43

Dense strong-motion instrument array in Sendai

44

Strong-motion instrument network in the Metropolitan Area

45

Strong-motion observation at Urban Disaster Prevention Research Center

45

Chapter 4oConclusion and Recommendation

47

oReference48

ACRONYMS

AFAD

Disaster and Emergency Management Presidency

ADRC

Asian Disaster Risk Reduction

BRI

Building Research Institute

EAFZ

East Anatolian Fault Zone

ERI

Earthquake Research Institute

GHAE

Great Hanshin-Awaji Earthquake

GEJE

Great East Japan EarthquakeJMA

The Japan Meteorological Agency

MoI

Ministry of Interior

NAFZ

North Anatolian Fault Zone

NIED

National Research Institute for Earth Science and Disaster Prevention

TR_NSMN

National Strong Motion of Turkey

YGF

The Yenice-Gonen Fault

ACKNOWLEDGEMENTS
I would like to express my deepest gratitude to the governments of both Japan and Turkey in givingme the tremendous opportunity to participate in this program.
Especially my thanks and best regards to all of those who devoted their time and efforts to educationand training in the field of disaster management.
And finally, I would like to express my appreciation to the ADRC staff, who made my time in Japan anexperience that has far surpassed my every expectation.

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CHAPTER 1
Introduction
Turkey between 35-42 north latitude, and 25-44 east longitude covers 779,452 sq km and has borders
with Bulgaria, Greece, Georgia, Armenia, Iran, Iraq and Syria. The road distance from Edirne on the
Bulgarian border to Kars on the Armenian one is over 1700 km. The coastlines along the Black, Aegeanand Mediterranean Seas total almost 8400 km. The country is geographically diverse, with snow-cappedmountains, rolling steep broad rivers, long rocky shorelines and rich agricultural valleys. Going from west
to east the climate changes from Mediterranean climate (sub-tropic) to hot and dry in summer and very
cold in winter. Rainfall along the Black Sea coast where the mountains come right down to the sea is twoto three times the national average.
Turkey is a bridge between east and west
geographically and have a socially, economically,and strategically vital role in the region. Turkey
has a population approaching 70 million. Since1980’s the population growth rate has been
decreasing from almost 3% to 2%. The most of the
population (67%) lives in cities. Two-thirds of the
population is under 25 years old.
GDP per capita 6.700 US$ (2003 estimation)
Sectoral distribution of GDP, for agriculture
11.7%, industry 29.8%
Turkey is progressing to overcome its present
difficulties. Its economy through many respects prosperous and dynamic, is saddled with a heavy burdenof debt and deficit, inflation and unemployment. Turkey has embarked on some ambitious projects inrecent years. There is a host of new roads, bridges, tunnels, dams, factories and universities. Due toglobalization and new economic policies Turkey approached to open market economy. The foreign tradecapacity reached to US$ 86 billion in 2002. The highest proportion in GDP is the industrial sector that has
a proportion increased to 28%, the agricultural sector’s proportion reached to 12% in 2003.

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There are 81 city provinces, 850 towns and 36,527 villages in Turkey. Almost 30% of total population lives
in the three-metropolitan cities (Istanbul, Ankara, Izmir). The dual organization of local administration in
Turkey, with appointed governors and elected municipal officials (mayors), establishes the basis for their
distinguished role in disaster management. Provincial governors are agents of the central authority,
therefore they conduct pro-active role in managing emergency situations as it stated in the Disaster Law7269. The mayor and municipal organizations stay under the authority of the governor in the emergency.
On the other hand, according to the Development Law-3194 land-use planning and building constructions
are administrated by the municipalities. The current compulsory earthquake insurance system, Turkish
Catastrophe Insurance Pool (TCIP) is running by an insurance administration (DASK) which is also
considered for leadership in mitigation activities to reduce losses, is relatively small, however, it has been
growing rapidly in recent years.
All of Turkey’s big cities are now ringed with settlements –gecekondu- inhabited by migrants from thecountryside who come looking for work. Many are escaping from the south-east Turkey where a burital
terrorism and also wars in the Gulf occurred. The absence of a public housing program, cheaply built,
illegal housing and the country’s poor inspection system contribute the problem in the major cities. For
Istanbul another most important and complex issue in mitigation is the retrofit of existing buildings.

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Risk Profile of Turkey
More than 95% of the country lies in one of the most active earthquake and landslide regions in the world.
Large earthquakes can occur anytime along the North Anatolian Fault Zone (NAFZ) which crosses theentire country. The ratios of events (left) and Affected Structures according to disaster types are shown
below.

There are 2 different major fault systems tectonically control Anatolia from east to west. the 1500-kmlong North Anatolian Fault Zone (NAFZ) and the 550-km long East Anatolian Fault Zone (EAFZ).

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 70% of the population lives in areas highly vulnerable to earthquakes.
 66% of the country is located on active fault zones.
 75% of damaged buildings and %64 of total disaster losses in the last century are due toearthquakes.
Population growth continues to increase development pressures that in turn lead to mostly uninsured
residential, commercial, and industrial poor construction in the alluvial plains (soft soil) along the NAFZ.
The resulting potential for social, economic, and devastation has been demonstrated time and again – e.i.
the 1999 Earthquakes.
The greatest landslide risk is within the Black Sea region. Due to climatic changes cities which are along
the rivers are at greatest risk from floods and landslides. Unfortunately, these regions are expose to floods
every year.
 Mostly in coastal plains and exacerbated by deforestation, erosion and ignorant development.
 15% of total disaster losses are due to floods.
 Annual average losses exceed 100 million US$
Most landslides are secondary hazards of earthquakes and floods.
 25% of country area is exposed to landslide hazard.
 11% of total population is located in landslide areas.
 16 % of total disaster losses are due to landslides.
In the last thirty years Turkey faced heavy natural disasters: e.g Erzincan Earthquake (1992), Flood in BlackSea Region (1998), Adana-Ceyhan Earthquake (1998), Marmara Earthquake (1999), Hakkari Earthquake(2004), Sivas Landslide (2005) and Van Earthquake (2011).
Direct economic losses due to natural disasters is expected 1% of GDP ever year. The losses like down inthe market, production losses and unemployment are even more greater. The probabilty of economic
losses exceeding 11.4 billion US$ in one year is about 0.5 percent. This is about 6% of the country’s GDP.
The probability of annual losses exceeding 3.5 billion US$ is about 5%.
For Istanbul, a worse-case scenario for earthquake of 7,5 is assume to take place along the Main Marmara
Fault of NAFZ. Probability of occurrence of a large earthquake in the next 30 years is greater than 65%, in
next 10 years is greater than 20%. Approximately 70 thousand dead people, 120 thousand heavily injured
people, 400 thousand injured, direct economic losses is 30 billion US$ (Erdik, 2003). Secondary impacts

Page | 9may be triggered by a large earthquake, liquefaction and subsidence of soil, landslides along the coastal
areas damaging transportation lines, infrastructure, fires from particularly natural gas pipeline ruptures.

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CHAPTER 2
Recent Major Earthquakes in Turkey
December 26, 1939 Erzincan Earthquake
The 1939 Erzincan Earthquake (M = 7.8), occurred on the NAFZ, was one of the most active strike-slip
faults in the world, and created a 360-km-long surface rupture. The 1939 Erzincan earthquake struckeastern Turkey at 1:57:23 a.m. on 27 December local time with a moment magnitude of 7.8 and amaximum Mercalli intensity of XII (Extreme). This was one of the largest in a sequence of violent shocks
to affect Turkey along the NAFZ between 1939 and 1999.

Almost 33,000 had died due to the earthquakes and to blizzard conditions, followed by heavy rains thatcaused floods. So extensive was the damage to Erzincan city that its old site was entirely abandoned anda new settlement was founded a little further to the north.
December 20, 1942 Erbaa Earthquake
Two devastating earthquakes occurred between Erzincan (39.75N, 39.49E) and Erbaa, Tokat (40.70N,
36.58E) just three years one after another in 1939 and 1942. While 1939 Erzincan earthquake (M=7.8)
ruptured nearly 360 km, 1942 Erbaa-Niksar earthquake (M=7.1) has a length of 50 km surface rupture.

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The 1942 Niksar–Erbaa earthquake in Turkey occurred at 16:03 local time on 20 December. It had anestimated surface wave magnitude of 7.0 and a maximum felt intensity of IX (Violent) on the Mercalli
intensity scale, causing 3,000 casualties.

November 26, 1943 Tosya-Ladik Earthquake
The 1943 Tosya–Ladik earthquake occurred at 00:20 local time on 27 November, near Tosya, Kastamonu
Province, in northern Turkey.

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The earthquake had an estimated moment magnitude of 7.5 and a maximum felt intensity of between IX–
X (Violent to Extreme) on the Mercalli intensity scale. It caused 2,824 deaths, 1250 injuries and about 75
percent of houses are destroyed or damaged in the Ladik-Vezirkopru area. The Earthquake produced 280
km long surface rupture in the Tosya-Ladik segment of the NAFZ.
February 1, 1944 Bolu-Gerede Earthquake
The 1944 Bolu–Gerede earthquake occurred at 05:22 local time on 1 February. The earthquake had anestimated surface wave magnitude of 7.2 and a maximum felt intensity of IX–X (Violent–Extreme) on
the Mercalli intensity scale. 2,790 people are killed and 50,000 houses destroyed or heavily damaged in
the NAFZ from Bolu through Gerede to Kursunlu.

May 31, 1946 Varto-Hinis Earthquake
The 1946 Varto–Hınıs earthquake occurred at 05:12 local time on 31 May. The earthquake had anestimated magnitude of 5.9 and a maximum felt intensity of VIII (Severe) on the Mercalli intensity scale,causing between 800 and 1300 casualties.

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March 18, 1953 Yenice-Gonen Earthquake
The tectonics of northern and eastern Turkey are dominated by the two strike-slip fault zones that
accommodate the west to southwestward movement of the Anatolian Plate relative to the Eurasian
Plate and the Arabian Plate as it is effectively being squeezed out by convergence between them. The
quake occurred along the Yenice–Gönen Fault (YGF), which is a southern extension of the North Anatolian
Fault Zone.
The YGF is located in the central part of the Biga Peninsula between Gönen and Yenice and is a rightlateral strike-slip active fault with general trending N65°E. On 18 March 1953 there was an earthquake on
the YGF that died 263 people (Ms=7.3) and a 70 km surface rupture developed during this earthquake.
The quake had a surface wave magnitude of 7.3 and it killed at least 1070; 998 of those deaths werein Yenice, with another 50 in Gönen, 20 in Çan, and 3 in Manyas. The cost of repair was estimated at
US$3,570,000. Several thousand buildings were affected in the Can-Yenice-Gonen area. Damage ofintensity VI occurred at Sakarya (Adapazari), Bursa, Edirne, Istanbul and Izmir.
The quake was felt throughout the Aegean Islands and in much of mainland Greece, with damage
occurring as far away as Crete. Shaking was also recorded in Bulgaria. Although officials predicted theearthquake would cause only 265 deaths, it multiplied with a death toll seven times the number as
expected.
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The damage caused by this earthquake led to a new national reconstruction law in Turkey. In Greece thedamage was severe enough that new building codes were introduced.
August 19, 1966 Varto Earthquake
The 1966 Varto earthquake occurred on 19 August with a magnitude of 6.8 a maximum Mercalli intensity
of IX (Violent). At least 2,394 were killed and up to 1,500 people were injured in the town of Varto in
the Muş Province of eastern Turkey.

The earthquake devastated all the structures in Varto. This disaster was preceded by an earthquake ofmagnitude 5.6 that hit Varto on 7 March 1966 killing 14 and wounding 75 people.
19 August 1966 Varto earthquake (Ms = 6.8) was an
extra ordinary event at the 40 km east of junction
between NAFS and EAFS which are two seismogenic
system and active structures shaping the tectonics ofTurkey. This earthquake sourced from Varto fault zone
which are approximately 4 km width and 43 km
length. It consists of faults which have parallel to subparallel, closely-spaced, north and south-dipping up to
85°-88° dip amount. Although this event has 6.8 (Ms)
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magnitude that is big enough to create a surface rupture, there was no clear surface deformation had
been detected. This creates the controversial issue about the source fault and the mechanism of theearthquake.
March 28, 1970 Kutahya-Gediz Earthquake
The 1970

Gediz

earthquake (also

known

as

the 1970

Kütahya-Gediz

earthquake)struckwestern Turkey on 28 March at about 23:02 local time, with an estimated magnitude of 7.2 on
the Ms scale. The event killed 1,086 people, injured 1,260 people, and left many thousands homelessin Gediz. A district of Kütahya Province situated 98 km southeast of Kütahya. Many people were burned
alive as fires broke out from overturned stoves, and 9,452 buildings in the region were severely damaged
or destroyed.

The town of Gediz, home to repeated natural disasters like earthquakes and floods, was relocatedfollowing a government resolution soon after the destruction to a new place 7 km away on the roadto Uşak under the name "Yeni Gediz" (literally: New Gediz). The residents moved in their newly
built, earthquake-resistant homes. Neighboring towns and villages were also rebuilt at places
with relative minimum earthquake risk. Other major earthquakes occurred in Gediz in 1866 and 1896,
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and on June 25, 1944, at 07:20 local time, a magnitude 6.0 earthquake occurred in Gediz, killing 20 people
and damaging around 3,500 buildings.

May 22, 1971 Bingol Earthquake
The 1971 Bingöl earthquake occurred at 18:44:02 local time on 22 May. It had a moment magnitude of
6.9 and a maximum intensity of VIII (Severe) on the Mercalli intensity scale, killing at least 755 people.

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September 6, 1975 Lice Earthquake
The 1975 Lice earthquake struck the Turkish district of Lice at 12:20 local time (09:20 UTC) on 6
September. The epicenter of the Ms 6.7 shock was located near the town of Lice and the maximum felt
intensity was VIII (Severe) on the Mercalli intensity scale. More than 2,300 people were killed.
The tectonics of Turkey are dominated by the effects of the continuing collision between the African
Plate and the Eurasian Plate. The main result of this collision is the southwestward escape of the Anatolian
Plate by displacement along the EAFZ and EAFZ. To the east of these faults, the plate boundary is a zoneof orthogonal collision, with the relative displacement spread out over a wide zone, continuing as far northas the Greater Caucasus. The largest fault within the plate boundary zone is the west-east trending Bitlis
frontal thrust and the 1975 earthquake is thought to have been caused by movement on this structure.
The earthquake occurred near midday without any warning. The shaking continued for about 20–24
seconds. The main shock was followed by aftershocks that continued for more than a month. The focal
mechanism for the earthquake suggests that it was associated with dominantly reverse movement on a
fault plane dipping at 45° to the northwest with a significant sinoatrial (left lateral) component.
The main area of damage was located near the towns of Hani, Lice and Kulp. In Lice 12 out of the
13 mahalles (sections) of the town were completely destroyed. 6 schools, 6 mosques and 132 commercial
buildings were damaged. In the 188 villages surrounding Lice that were affected, 5,555 houses sufferedeither severe damage or total destruction.

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November 24, 1976 Van-Caldiran Earthquake
The 1976 Çaldıran–Muradiye earthquake occurred at 14:22 local time (12:22 UTC) on 24 November.
The epicenter was located near Çaldıran, 20 km northeast of Muradiye, in the Van Province ofeastern Turkey. The earthquake had a magnitude of 7.3 with a maximum intensity of X on the Mercalli
intensity scale. The area of severe damage, where over 80% of the buildings were destroyed, covered anarea of 2,000 square kilometers. There were between 4,000 and 5,000 casualties.
The easternmost part of Turkey lies within the complex zone of continuing continental collision between
the Arabian Plate and the Eurasian Plate. The overall shortening that affects this area is accommodate
partly by thrusting along the Bitlis-Zagros fold and thrust belt and partly by a mixture of sinistral strikeslip on SW-NE trending faults and dextral strike-slip on NW-SE trending faults. The earthquake was causedby movement on the Çaldıran Fault, one of the dextral faults, which had not been recognised before theearthquake. No earthquakes with magnitudes of 6 or greater were recorded within 100 km of Çaldıran in
the preceding 74 years, possibly explaining why it was considered an area of only intermediate seismic
risk (zone 3 out of the five zone system of seismic risking used in Turkey at the time, with zone 1 being thehighest).
The earthquake was associated with a 50–55 km zone of surface faulting, extending from three kilometres
west of Sarikök in the west to just west of Baydoğan in the east. A maximum dextral offset of 3.5 m wasrecorded. The rupture width was estimated at 24 km and the fault zone was found to dip at 78° to thesouth. The duration of strong ground shaking is estimated at six seconds.
In Çaldıran 95% of the houses were destroyed with all the others damaged to some extent and 615 of the
3,304 inhabitants were killed.[4] In the villages around Çaldıran over 80% of the houses were destroyed
and most of the rest were damaged; 2,313 of the 27,587 inhabitants were killed. In Muradiye almost all
the houses were either completely collapsed or damaged and 159 of the 6,753 inhabitants were killed.

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Most of the buildings in the epicentral area were constructed of thick walls made from rubble masonry
cemented with mud mortar. The structures were typically finished with a heavy earth roof with wooden
supports. The very low resistance to lateral loads of these structures explains why almost all the buildingsin Çaldıran collapsed in the earthquake, causing most of the deaths. Reinforced concrete structuresgenerally performed well, with none suffering complete collapse. The performance of brick or stone
masonry structures was mixed, with some collapsing and others being apparently unaffected.

October 30, 1983 Erzurum earthquake
The 1983 Erzurum earthquake occurred on 30
October 1983 at 07:12 local time (04:12
UTC). It was an Ms 6.9 earthquake. About
1,340 people are killed and 530 injured when
an earthquake hits the Turkish city of Erzurumin the northeast. Measuring 6.9, 50 villages aredestroyed in the provinces of Erzurum andKars.

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August 17, 1999 Izmit Earthquake
The 1999 İzmit earthquake (also known as the Kocaeli, Gölcük, or Marmara earthquake) occurred on 17
August at 03:01:40 local time in northwestern Turkey. The shock had a moment magnitude of 7.6 and amaximum Mercalli intensity of IX (Violent). The event lasted for 37 seconds, killing around 17,000
people and left more than 250,000 people homeless. The nearby city of İzmit was severely damaged.
The earthquake occurred along the western portion of the NAFZ. The Anatolian Plate, which consists
primarily of Turkey, is being pushed west about 2–2.5 cm (0.8–1.0 in) a year, as it is squeezed between
the Eurasian Plate to the north and the Arabian Plate to the south. Major earthquakes in Turkey result
mainly from slip along the NAFZ or the EAFZ.
The Izmit earthquake had a rupture length of 150 kilometers (93 mi) extending from the city of Düzce all
the way into the Sea of Marmara along the Gulf of İzmit. Offsets along the rupture were as large as 5.7
meters. From the timing of P-wave and S-wave arrivals at seismometers there is strong evidence that therupture propagated eastwards from the epicentre at speeds in excess of the S-wave velocity, making thisa supershear earthquake.

Destruction in Istanbul was concentrated in the Avcılar district to the west of the city. Avcılar was built on
relatively weak ground mainly composed of poorly consolidated Cenozoic sedimentary rocks, whichmakes this district vulnerable to any earthquake.

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The earthquake was heavily felt in this industrialized and densely populated urban area of the country,
including oil refineries, several automotive plants, and the Turkish navy headquarters and arsenal
in Gölcük, increasing the severity of the loss of life and property. The earthquake also caused considerable
damage in Istanbul, about 70 kilometers away from the earthquake's epicenter.
Totally at 17,127 killed and 43,959 injured, butmany sources suggest the actual figure may havebeen closer to 45,000 dead and a similar number
injured. Reports from September 1999 show that
120,000 poorly engineered houses weredamaged beyond repair[citation needed] andapproximately 20,000 buildings collapsed,
resulting in more than 250,000 people becoming
homeless after the earthquake.
There was extensive damage to several bridges and other structures on the Trans-European Motorway(European route E80), including 20 viaducts, 5 tunnels, and some overpasses. Damage ranged fromspalling concrete to total deck collapse.

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The earthquake sparked a disastrous fire at the Tüpraş petroleum refinery. The fire began at a stateowned tank farm and was initiated by naphtha that had sloshed out of a holding tank. Breakage in water
pipelines, results of the quake, nullified attempts at extinguishing the fire. Aircraft were called in to douse
the flames with foam. The fire spread over the next few days, warranting the evacuation of the area within
three miles of the refinery. The fire was declared under control five days later after claiming at least
seventeen tanks and untold amounts of complex piping. The earthquake caused a tsunami in the Sea ofMarmara that was about 2.5 meters high. The tsunami caused the deaths of 155 people.
Oct 23, 2011 Van Earthquake
The 2011 Van earthquakes occurred in eastern Turkey near the city of Van. The first earthquake
happened on 23 October at 13:41 local time. The shock had a Mw magnitude of 7.2 and amaximum Mercalli intensity of VIII (Severe). It occurred at a shallow depth, causing heavy shaking acrossmuch of eastern Turkey and lighter tremors across neighboring parts of the South Caucasus and Levant.
According to Disaster and Emergency Management Presidency on 30 October, the earthquake killed 604
and injured 4,152. At least 11,232 buildings sustained damage in the region, 6,017 of which were foundto be uninhabitable. The uninhabitable homes left as much as 8,321 households with an average
household population of around 7.6 homeless in the province; this could mean that at least around 60,000
people were left homeless. The other 5,215 have been damaged but are habitable. A separate earthquake

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within the same earthquake system happened on 9 November at 21:23 local time (19:23 UTC). 40 people
were killed and 260 people were injured in the 9 November earthquake.
The magnitude 7.2 (Mw) Eastern Highlands
earthquake occurred inland on 23 October
2011 at 13:41 local time (EEST), centeredabout 16 kilometers north-northeast of Van,
Turkey and at an estimated focal depth of 7.2
kilometers. Its focal region and much ofeasternmost Turkey lie towards the southernboundary of the complex zone of continental
collision between

the Arabian

Plate andthe Eurasian Plate, beyond the eastern extent of the Armenian and Asia Minor fault zones. Part of theconvergence between these two plates takes place along the Bitlis-Zagros fold and thrust belt. The
earthquake’s focal mechanism indicates oblique thrust faulting, consistent with the expected tectonics inthe region of the Bitlis-Zagros Fault Zone, where thrust mechanisms dominate.

The size of the rupture has been estimatedas 60 km x 20 km, consistent with theobserved distribution of aftershocks, on a
WSW-ENE orientated fault plane with a dipof about 35°. An offset of about 2 meters
has been estimated at 10–15 kilometers
depth but there is no visible rupture of theground surface. The rupture lasted forabout 50 seconds.

There have been 1,561 aftershocks above magnitude 2.0 as of 30 October. The highest magnitudeaftershock came at 11:45 pm Local on 23 October, with a MI 5.7 and Mw 6.0. The number of aftershocks
reported in ranges as follows: 556 ranging from magnitude 2 to 3; 832 ranging from magnitude 3 to 4; 108

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ranging from magnitude 4 to 5; and 7 ranging from magnitude 5 to 6. In the first five months there were
9,367 aftershocks with magnitudes in the range 1.5 to 5.8.

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National Strong-Motion Network of Turkey (TR-NSMN)National Strong-Motion Network of Turkey (TR-NSMN) was established in 1973 with 67 analog recorders
and recorded the first strong-ground motion record in 1976. Digital accelerometer devices have been
installed since 1993. In 2014, TR-NSMN started to record data in a real-time (online) mode under anational Turkish Earthquake Data Center Project (TDVM-2013) conducted by Disaster and Emergency
Management Authority (AFAD).

Recently, TR-NSMN with 678 stations in total consists of 3 different digital tri-axial force-balanceaccelerometers of CMG-5TD (24 bit) at 338 stations), SARA (24 bit) at 115 stations, GSR (16/18 bit) at 8
stations, and GMSplus (24 bit) at 217 stations.

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All the accelerographs are located on the free surface in densely populated cities in active regions such as
NAFZ, EAFZ and the Aegean Graben Systems. Data transmission is provided via dial-up, ADSL, GPRS EDGE
(mostly) and satellite. All the records are stored in an ASCII format including N-S (north-south), E-W (eastwest) and U-D (up-down) components and there isn’t any process implemented on the acceleration data,
except for a base-line correction.

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The data coming from field are transmitted to thedata center by means of Dial-Up, ADSL, GPRS andSatellite. Data transferring is mostly provided via
GPRS (EDGE).

As site conditions of the strong-ground motion stations, shallow S-wave velocity structures (for the first
30 meters) were obtained at many of the stations (Akkar et al., 2010; Sandıkkaya et al., 2010; Yılmaz etal., 2008). Additional S-wave data at some of the stations were available in geophysical explorations, suchas microtremors (e.g., Özmen et al., 2017b; Yamanaka et al., 2018).

Since the establishment of TR-NSMN data center (1973), it is possible to access to all accelerograms on
the web site (www.deprem.gov.tr).
File names are generated and saved as in this example:
Date (yyyymmdd)+time(hhmmss)+abbreviation of the station (1201)(ex.20030501002704_1201).

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All records are created as ASCII format as seen in Figure 9. Beneath the header information there are threecomponents of acceleration data like; N-S (North-South), E-W (East-West) and U-D (Up-Down). Besides,
sample interval value for each record can be found in the header information. There isn’t any process
implemented on acceleration data, except for base-line correction, in the other words, records on the
web page are entirely raw data and unit of PGA values is cm/sn2 (gal).

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Local Networks
Local networks have also been operated within the framework of the different projects or cooperation.
These are deployed with specific geometrical arrays on active fault systems in order to observe seismic
activity closely. Currently, with different regions and arrays, 10 local- scale networks around the
populated cities located very close to active faults have been operated under the TR-NSMN. The first one
is, supported by the NATO Science for Peace Program (SFP977484) in 2001, procured with 20 instruments
around two arrays (Gülkan et al. 2007). One of these array has already been positioned between Yalova
and Bursa (BYT-NET: 27) region in north-western and the other one is between Aydin and Denizli (DATNET:
18) region in western of Turkey. In addition to these, between Hatay and K.Maras region (MAT-NET: 55),
in Eskişehir (ANA-NET: 15), in Kocaeli (KOC-NET: 25), in Antalya (ANT-NET: 14) and in Düzce (DUZ-NET: 8)
provinces are the others. Another important local array, İZMİR-NET, which consist of 32 stations installedin İzmir province with TUBİTAK support (Polat et al. 2009). The last of these arrays, KKTC-NET (13) andIskenderun (ISK-NET: 10) have been connected to the national network in 2012. Locations of the local
networks are shown in Figure 8. In time, all local networks have been enhanced in terms of both number
and instrument quality.

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Apart from local networks, within the framework of the AFAD RED Project (Rapid Loss Estimation Project)
20 accelerometers have been installed both K.Maraş and Hatay provinces in 2013. While installing it,
conditions such as density of buildings and population, different sites and geological units etc. wereprimarily taken into consideration. Initiated for a specific purpose, scope of this project will be extended
and will be implemented at the various regions in 2014 as well.

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CHAPTER 3
Recent Major Earthquakes in Japan
Japan has a notorious earthquake history. About 1,500 earthquakes strike the island nation every year.
Minor tremors occur on a nearly daily basis. Deadly quakes are a tragic part of the nation's past.
Japan has such a large potential for earthquakes anddisaster because the nation sits atop four huge slabsof the Earth's crust, called tectonic plates. These
plates mash and grind together and trigger deadly
earthquakes, like the 9.0-magnitude quake thatstruck on March 11.

September 1, 1923 Great Kanto Earthquake
In 1923, a magnitude 7.9 earthquake struck the Kanto plain on the island of Honshu on the morning ofSept. 1. The shaking lasted up to 10 minutes in some places. The quake devastated Tokyo, then home toabout 2 million people, and caused widespread damage throughout the Kanto region.
The earthquake triggered massive fires (people
were cooking lunch on gas stoves when thequake hit). The after-fires claimed far more lives
than the earthquake itself. The quake killed
142,800, making it one of the deadliest of alltime.
In remembrance of the earthquake, September
1st is Disaster Prevention Day in Japan.

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March 2, 1933 Sanriku Earthquake
The 1933 Sanriku earthquake occurred on the Sanriku coast of the Tōhoku region of Honshū, Japan on
March 2 with a moment magnitude of 8.4. The associated tsunami caused widespread damage to towns
on the Sanriku coast of the Tohoku region of Honshu, killing more than 3,000.

Although little damage was produced from the shock, the tsunami, which was recorded to reach theheight of 28.7 metres at Ōfunato, Iwate, caused extensive damage, and destroyed many homes andcaused numerous casualties. The tsunami destroyed over 7,000 homes along the northern Japanese
coastline, of which over 4,885 were washed away. The tsunami was also recorded in Hawaii with a heightof 9.5 feet, and also resulted in slight damage. The death toll came to 1,522 people confirmed dead, 1,542
missing, and 12,053 injured. Hardest hit was the town of Tarō, Iwate (now part of Miyako city), with 98%
of its houses destroyed and 42% of its population killed.
December 20, 1946 Nankaido Earthquake
A magnitude 8.1 earthquake struck Nankaido, Japan, on Dec. 20, 1946. The earthquake was felt from
Northern Honshu Japan's largest island and home to about 100 million people to the southernmost islandof Kyushu. The quake killed 1,362 people.

Page | 33

This quake ruptured in the Nankai Trough, a subduction zone where one tectonic plate slides below
another. Earthquakes have been rupturing here every 100 to 200 years since the 7th century.
May 16, 1968 Tokachi Earthquake
The 1968 Tokachi earthquake occurred on May 16 at 0:49 UTC(09:49 local time) in the area offshore Aomori and Hokkaido.
The magnitude of this earthquake was put at Mw 8.3. The
intensity of the earthquake reached shindo 5 in Aomori,
Aomori and Hakodate, Hokkaido.
The source region of this interplate earthquake covered abroad stretch in the open sea east of Aomori Prefecture.
Strong ground motion was felt over a wide area, primarily inthe northern Tohoku region and southern Hokkaido. In the
Tohoku region, this earthquake registered a seismic intensityof 5 in JMA scale in Aomori City and Hachinohe (Hatinohe) City. This earthquake also generated a tsunamithat was around 6 m at its highest point. The tsunami arrived at low tide, however, so only slight damage
resulted.

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The earthquake was responsible for a total of 52 fatalities, 47 of which were in Aomori Prefecture. The
primary damage included landslides and the collapse of cliffs and houses. Damage was extensive in areas
with soft ground, including hilly areas comprised of volcanic deposit, reclaimed land, and low marshy
areas. Another factor thought to have contributed to the damage was the soft ground caused by morethan 200 mm of rainfall in three days prior to the event in eastern Aomori Prefecture.
The largest aftershock (M 7.5) occurred about 12 hours
after the main shock on May 16 and the M 7.2 aftershock
occurred on June 12. Seismic intensity 4 in JMA scale wasobserved over a wide area from the northern Tohoku region
to southern Hokkaido. The largest aftershock, which
occurred on May 16, registered a seismic intensity of 5 in
JMA scale in Urakawa and Hiroo in southern Hokkaido. The
frequency of aftershocks increased for a time on June 12,
but gradually diminished .
The 1952 Earthquake off the Coast of Tokachi (M 8.2)
occurred in the area adjoining the northeast side of the siteof the 1968 Earthquake off the Coast of Tokachi.

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January 17, 1995 Great Hanshin-Awaji Earthquake
The Great Hanshin earthquake occurred on Tuesday, January 17, 1995, at 05:46 JST (January 16 at
20:46 UTC) in the southern part of Hyogo Prefecture, Japan. It measured 6.8 on the moment magnitude
scale (USGS) and Mj7.3 (adjusted from 7.2) on JMA magnitude scale. The tremors lasted forapproximately

20

seconds.

The focus ofearthquake

waslocated

16 km

the

beneathits epicenter on the northern end of Awaji Island,
20 km away from the city of Kobe.
It killed 6,434 people; injured 43,792; destroyed
104,906 houses; half destroyed 144,274 houses;and partially destroyed 390,506 houses. The fires
that broke out because of the earthquake burned
down an area of 835,858 square meters.
November 15, 2006 Kuril Islands Earthquake
The 2006 Kuril Islands earthquake occurred on November 15 at 8:14:16 pm JST with a Mw magnitude of
8.3 and a maximum Mercalli intensity of IV (Light). This megathrust earthquake was the largest event in
the central Kuril Islands since 1915 and generated a small tsunami that affected the northern Japanese
coast.

The

tsunamicrossedthe Pacific Ocean and damaged theharbor at Crescent City, California.
Post-tsunami surveys indicate thatthe local tsunami in the central Kuril
Islands reached run-up of 15 meters
or

more.

This

earthquakeisconsidered a doublet of the 2007
Kuril Islands earthquake that hit thesame area on January 13, 2007.

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March 11, 2011 Great East Japan Earthquake
The 2011 earthquake off the Pacific coast of Tohoku, also known as the 2011 Tohoku earthquake or theGreat East Japan Earthquake, was a magnitude 9.0 (Mw) undersea megathrust earthquake off the coastof Japan that occurred at 14:46 JST (05:46 UTC) on Friday, 11 March 2011, with the epicenter
approximately 70 kilometers (43 mi) east of the Oshika Peninsula of Tohoku and the hypocenter at anunderwater depth of approximately 30 km (19 mi).
It was the most powerful known earthquake
ever to have hit Japan, and one of the five mostpowerful earthquakes in the world overall sincemodern record-keeping began in 1900. The
earthquake triggered powerful tsunami waves,which reached heights of up to 40.5 meters(133 ft) in Miyako in Tōhoku's Iwate Prefecture,
and which in the Sendai area travelled up to
10 km (6 mi) inland. In addition to loss of life anddestruction of infrastructure, the tsunami caused a number of nuclear accidents, primarily the ongoinglevel 7 meltdowns at three reactors in the Fukushima I Nuclear Power Plant complex, and the associatedevacuation zones affecting hundreds of thousands of residents.

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Strong Earthquake Motion Observation in Japan
In the light of the tragic disaster of the 1995 Hyogo-ken-nanbu (Kobe) Earthquake, the Special Measure
Law on Earthquake Disaster Prevention (implemented on July 18, 1995) was passed to protect thepeople's lives and properties from disasters caused by earthquakes. According to the law, theHeadquarters for Earthquake Research Promotion was established under the Prime Minister's Office forunified promotion of earthquake research.
The Headquarters is comprised of the Director (Minister of State for Science and Technology) and its staff(Vice-Ministers of relevant Ministries and Agencies). Under the Headquarters, there are two subsidiarycommittees, each is comprised of the staffs of relevant Ministries and those of people of experience or
academic standing, who are conducting the following mandate concerning to earthquake research.
 Planning comprehensive and basic policies,
 Coordinating administrative works such as budgets for relevant bodies, Formulating comprehensive survey and observation plans, Collection, arrangement, analysis and comprehensive evaluation of the results of surveys by
relevant administrative bodies and universities, Public relations based on the comprehensive evaluations.
On the other hand, the situation of strong motion observation also underwent drastic changes. Several
projects were planned and conducted in order to reinforce the strong motion network. Japan
Meteorological Agency (JMA) deployed about 600 seismic intensity meters throughout Japan. National
Research Institute for Earth Science and Disaster Prevention (NIED) established the nationwide network"K-Net" with 1,000 observation sites. NIED is also constructing another strong motion instrument network"KiK-Net". Every prefecture equipped the seismic intensity information network system to concentrate
data from all containing municipalities. About 2,600 seismic intensity meters were newly installed inmunicipalities that have neither JMA station nor K-Net station. Those up-to-date networks can gather andannounce the seismic information rapidly.
The Japan Meteorological Agency (JMA) Seismic Intensity Network
The Japan Meteorological Agency (JMA) is a unique national agency that is responsible for tsunami
forecasts, short-term prediction of a large earthquake, and information service on earthquakes, tsunamis
and volcanic activities. JMA is operating a network made up of about 180 seismographs for continuous
earthquake monitoring and 600 seismic intensity meters covering the whole of Japan as shown in Figure.
Page | 38

The Earthquake Phenomena Observation
System (EPOS) at the headquarters of JMA in
Tokyo and the Earthquake and Tsunami
Observation System (ETOS) at six District
Meteorological Observatories collect theobservational data.
After

an

earthquake

occurs,JMA

immediately processes the observational
data and quickly announces information on
epicenter, magnitude and the distribution ofseismic intensity to the public through themedia as well as to the disaster prevention
organizations. Information from 2,000 seismic intensity meters, which are set up by local governments, isalso compiled together.
The JMA seismic intensity scale was originally assessed by the human feeling and the damage
examination. In 1996, JMA introduced the new seismic intensity scale, which can be calculated fromacceleration records, and developed the seismic intensity meter for prompt estimation of the
instrumental seismic intensity. Table provides situation and damage caused by earthquakes
correspondent to the JMA seismic intensity scales. Acceleration data files are distributed by Japan
Meteorological Business Support Center at cost later on.

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K-Net and KiK-net
National Research Institute for Earth Science and Disaster Prevention (NIED), Science and Technology
Agency, constructed a large network, which is called K-Net e), of strong motion instruments in 1996. KNET consists of 1,000 observation stations that were deployed all over Japan with spaces of about 25 km.
Each station has a digital strong-motion instrument with a broad frequency-band and a wide dynamic
range on the free field and connects with the control center in NIED, Tsukuba, through the Integrated
Services Digital Network (ISDN) line. After the occurrence of an earthquake, the distribution of peakground accelerations is quickly reported by facsimile and e-mail. Digital acceleration records are postedon the web site within a few days.
NIED is also deploying the highsensitivity seismograph (Hi-net)
and the digital strong-motion
seismograph (KiK-net) across theall of Japan, as part of theactivities of the Headquarters for
Earthquake Research Promotion.
A high sensitivity seismographand an acceleration sensor are
installed on the firm bedrock at
the bottom of a well. An
additional acceleration sensor isplaced on the ground surface. The
project plans to construct a
network of more than 500
stations, and about 450 installations have been completed at present. Strong earthquake motion data areopened on the Internet web server.
Seismic Intensity Information Network of Local Governments
The Fire Defense Agency, Ministry of Home Affairs, subsidized local governments to construct the network
system that gathers information on seismic intensity promptly. The system assists emergency measuresand disaster relief activities by transmitting the information to organizations concerned with disastermeasures. A seismic intensity meter is installed in every municipality and each local government collects
Page | 40

seismic intensities from containing municipalities. All information finally concentrates at the Fire Defense
Agency. About 200 JMA stations and 500 K-Net stations have been already placed on the premises ofmunicipal offices. Therefore, 2,600 seismic intensity meters were newly installed at remaining
municipalities. Forty-seven local governments (prefectures) and about 3,300 municipalities (cities, towns
and villages) are enrolled in this huge network in total. Seismic intensity scales at a large part of thestations are included in the JMA announcement.

Other National Research Institutes and Public Bodies
Public Works Research Institute, Ministry of Construction
Public Works Research Institute (PWRI), Ministry of Construction, is a national institute in the field of civilengineering. PWRI developed an essential tool for grasping damage outline immediately after anearthquake by providing rough estimation on damage of road facilities. The tool, which is called Seismic
Assessment Tool for Urgent Response and Notification (SATURN), consists of about 700 strong motion
instruments placed along highways and rivers with an interval of 20 to 40 kilometers 3). Peak groundaccelerations and spectrum intensities are transmitted to the headquarters in real-time, and are used toestimate liquefaction possibilities and damage of highway bridges.
On the other hand, PWRI is operating the Dense Instrument Arrays for Strong Motion Monitoring in ninesites. In order to investigate the seismic effect of geological and topographical conditions, many
accelerometers are three-dimensionally arrayed at each site. PWRI is also maintaining traditional strong
Page | 41

motion observation sites. The network possesses 1672 instruments at 361 sites and targets dynamic
behavior of bridges, river embankments and dams.
Port and Harbour Research Institute, Ministry of Transport
Port and Harbour Research Institute (PHRI), Ministry of Transport, is committed to researching on broad
range of themes concerning ports and harbors as well as airports by tying-up closely with the bureaus of
the ministry in charge of constructing ports and airports. Strong motion observation of PHRI has been
carried out since 1963, and nowadays observation stations reach 57 ports including high-density
earthquake observation network using seismic meter distributed intensively in the Haneda Airport andthe Kushiro Airport 6). The results of the observation are periodically reported as the annual reports andwidely used for seismic design and study on earthquake disaster prevention measures.
Earthquake Research Institute (ERI), University of Tokyo
Earthquake Research Institute (ERI), University of Tokyo was a member institute of the Strong Motion
Accelerometer Committee that developed the original Japanese strong motion instruments, and has long
history of strong motion observation. ERI has deployed strong motion observation stations from southern
Kanto area to Suruga Bay, and densely arranged instruments in the Ashigara Plain as shown in Figure.
Observational records are provided on the Internet web site.

Tokyo Gas Co. Ltd.
Tokyo Gas Co. Ltd. supplies gas to customers in the Tokyo metropolitan area. Tokyo Gas launcheddevelopment of the Seismic Information Gathering and Network Alert System (SIGNAL) in 1986 and put it
into operation with 331 SI (Housner's Spectral Intensity) sensors in 1994. In addition, Tokyo Gas
Page | 42

commenced preparation of the most extensive ultra-high-density real-time seismic motion monitoringand disaster mitigation system in 1998. The system, which is called Super-Dense Real-Time Monitoring ofEarthquakes (SUPREME), will install 3,600 new SI sensors.
Yokohama City
Yokohama City, the second largest city in Japan, founded the Dense Strong Motion Network as a part of
the READY (Real-time Assessment of Earthquake Disasters in Yokohama) system. The network consists of
150 ground surface stations and nine borehole stations distributed at an average interval of 1.7
kilometers. Information on earthquake ground motions, e.g. peak ground acceleration and JMA seismic
intensity, is transmitted to three centers through the ISDN line within three minutes.
The seismic information is reported to organs concerned disaster countermeasures and is utilized fordamage estimation by READY. Distribution of seismic intensity is also uploaded to the web site of
Yokohama City.
Building Research Institute (BRI)
Building Research Institute (BRI), Ministry of Construction, is a national institute engaging in researches
on architecture and building engineering. BRI has started the installation of strong motion instruments
more than 40 years ago and is now in charge of three networks. The aim of the observation is contribution
to the enhancement of earthquake-resistant design technology by means of experimental investigationof strong ground motion characteristics and building seismic response. Dynamic soil-structure interactionis also the essential target of observation. Our three networks and the intensive strong motion installation
at BRI are outlined hereinafter.
Nationwide Strong Motion Network
The nationwide strong motion network, which has the longest history, has observation sites in major cities
throughout Japan. Forty-seven observation sites are equipped with digital strong-motion instruments asshown in Figure , and connected to BRI through the telephone line. The objects of observation are mainly
buildings, and acceleration sensors are usually placed both at the top floor and at the basement floor of
the building. In addition, a sensor is also set up on the ground surface at the newly equipped sites.
The network has obtained a number of noteworthy records. For example, in the 1964 Niigata Earthquake,the change in the characteristics of the seismic motion caused by liquefaction was clearly recorded in thebuilding next to the collapsed apartment house in Kawagishi-cho. Also, in the 1978 Miyagi-ken-oki (OffMiyagi Pref.) Earthquake, acceleration of more than 1,000 cm/s2 was recorded at the top floor of thenine-story school buildings of Tohoku University. Recently, the peak ground acceleration of 711 cm/s2 wasPage | 43

recorded at the Kushiro Local Meteorological Observatory by the 1993 Kushiro-oki (Off Kushiro)
Earthquake. In addition, in the 1994 Sanriku-haruka-oki (Far Off Sanriku) Earthquake, an enormous
acceleration record was obtained in the building next to the severely damaged old Hachinohe city hallbuilding.

Dense strong-motion instrument array in Sendai
It has been considered that the sub-surface layer especially influences characteristics of the seismic
motion acting upon buildings. From 1984 to 1989, eleven observation stations were established on
grounds with various conditions in the Sendai area, under the name of joint research by governmental
and private bodies. Each observation station holds three accelerometers, placed on the ground surface,in the base rock, and in the intermediate
layer. Figure shows configuration ofobservation stations.
The observation systems of all stations arecollectively controlled by the control centerin Sendai City. An NTT exclusive line
connects the observation stations with thecontrol center, and an NTT public line
connects the control center to BRI in
Page | 44

Tsukuba. The information on the earthquake records and the change of instrumental conditions will besent immediately.
The project as joint research with private bodies has been completed in 1999. BRI reduced the network
and updated recording equipment in order to continue the operation.
Strong-motion instrument network in the Metropolitan Area
The 1995 Hyogo-ken-nanbu (Kobe) Earthquake awakened us again to the importance of disasterprevention measures for large-scale urban areas. It is important to predict the probability of a futureearthquake and its impact, and make as many preparations as possible in anticipation of such an event. It
is also very essential to grasp the damage situation immediately to put in effect the necessary
countermeasures.
In

1996,

BRI

establishedeighteennewobservation sites that are deployed radially in theTokyo metropolitan area as shown in Figure.
Tokyo stands on the extremely thick sediment at
the center of the Kanto Plan, which is the largest
on in Japan. Therefore, the site configuration wasplaned in consideration of the effect of thesedimental layers and the influence of extensive
Kanto Plain on seismic motions. At typical sites,
two or three accelerometers are installed in abuilding. The system immediately collects
information on the seismic intensities through the telephone line at the time of an earthquake occurrence.
Strong-motion observation at Urban Disaster Prevention Research Center, BRI
The project to observe the complicated behavior of the building and the effect of the soil-structureinteraction during earthquakes was drafted with the construction of the Urban Disaster Prevention
Research Center building of Building Research Institute, Tsukuba. The installation was completed in 1998,
and the observation is now under way.
The annex building has eight stories with single basement floor and supported by the mat foundation on
the clayey layer of 8.2 meters below. The observation system has eleven sensors in the annex building,seven sensors in the surrounding ground, and four sensors in the main office building. The farthest sensor

Page | 45

on the ground is placed 100 meters away fromthe annex building, and the deepest sensor is set
up 89 meters in depth.
The amplification process by the ground surface
layers and the three-dimensional behavior of
the buildings are recorded using twenty-two
sensors in total. All sensors are connected to therecording equipment in the observation room in
the annex. The system has 24-bit A-D
converters, high-performance digital signal
processors and 40 MB flash memory storage.

Page | 46

CHAPTER 4
Conclusion an Recommendations
History of strong motion observation reaches a half of a century in Turkey. The instrumentation
technology has been steeply improved and the observation density has been extremely getting higher.
Especially the 1999 Izmit Earthquake accelerated installation of strong motion instruments as a principal
part of the real-time disaster information system
On the other hand as in the case of Japan; information on the intensity of earthquake motions is gatheredprimarily. Peak ground accelerations, JMA seismic intensity scales and/or SI values are adopted as values
representing the ground motion intensity. Acceleration wave data will be afterwards collected.
Characteristics of recent strong motion instruments and observation work in Japan can be summarized asfollows:
 High reliability and broad dynamic range of instruments,
 Calculation and display of seismic intensity scale and/or spectral intensity, Prompt transmittance and announcement of seismic information,
 Mutual use of seismic information between different networks, Rapid publication of digital acceleration data, Utilization of Internet
In the light of this information; it is suggested that TR-NSMN should be developed as in the case of Japan.
However, as is known the most of strong motion instruments which were expanded after the 1999 Izmit
Earthquake are placed on the ground surface.
On the other hand, strong motion observation for structures is also essential to rationalization of seismic
design. More reinforcement of the strong motion observation targeted at building structures is earnestly
expected.

Page | 47

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