Individual Training Course"Seismic Microzonation"
ReportAuthor:
Evgheni Isicico

Institute of Geophysics and Geology
Moldavian Academy of Sciences

December 2004

CONTENT
1. Local Site Conditions Modeling on Seismic Microzonation Stage ..........................................3
1.1. Introduction.........................................................................................................................3
1.2. Geometrical parameters of model.......................................................................................5
1.3. Elastic properties of model ...............................................................................................10
1.4. Comparison of amplitude-frequency characteristics of modeling and real sites ..............13
1.5. Comparison of modeling characteristics and H/V ratio of microtremors spectra ............15
1.6. Amplification properties of sites.......................................................................................17
1.7. Resonance properties of sites............................................................................................20
Conclusion ...............................................................................................................................23
2. Study trips ...............................................................................................................................242.1. Study trip to Kochi............................................................................................................24
2.2. Study trip to Fukuoka, Kyushu University .......................................................................25
2.3. Study trip to Hokkaido......................................................................................................26
2.4. Study trip to Kobe.............................................................................................................34
2.5. Study trip to Yokohama, Kanagawa University ...............................................................35
3. Lecture course in BRI, IISEE and other activity in Tsukuba..................................................41
Gratitude......................................................................................................................................422

1. LOCAL SITE CONDITIONS MODELING ON SEISMICMICROZONATION STAGE
1.1. Introduction
The basic task of modeling in our case is the reception of continuous 3D geophysicalmodel of site conditions for territory Kishinev city. For this purpose it is necessary to know
geometrical parameters of distribution of separate layers and their elastic properties, both on thearea, and with depth. The modeling usually is the compelled measure, owing to ourfragmentary knowledge of geological medium and is based therefore, as a rule, on averaging ofgeometrical and elastic parameters of layers. In other words, inevitable attributes of modelingare simplification of geological layers and averaging of elastic properties in them. It is natural,that the degree of a divergence of real seismic effects observable on a surface, from simulated
entirely is explained by differences of local site conditions from averaged, used in model.
For last 50 years on Kishinev city sizeable volume of the geological, hydro-geologicaland geophysical data was assembled. It has allowed to create continuous simplified 3D-modelof site conditions for territory of city. And then to use it as a basis for creation of a map ofseismic microzonation. All cartographic drawing and calculations are executed with use of GIS
technologies
The territory of city represents a valley with hilly slopes. The absolute heights from sea
level change within the limits of 30-230 m (fig. 1.1). The area of city is equal 122,3 sq. km.
In fig. 1.2 points of seismic observation (21 - earthquakes, 45 - special explosions, 143– microtremors) and 2673 boreholes (from which 1045 - geotechnic, 118 – seismic boreholelogging) are shown.

3

Fig. 1.1. Relief of Ground Surface

Fig. 1.2. Map of observation data4

1.2. Geometrical parameters of model
The geometrical parameters of model were determined with the help of maps of various
layers and geological cross-sections made on the data of drilling 2673 boreholes. In figures 1.3
and 1.4 the geological cross-sections on lines IV and XI are shown, giving representation about
a geological structure of territory.

Fig. 1.3. Geological cross-section (line VI)

Fig. 1.4. Geological cross-section (line IX)

5

The bedrock of cross-sections is limestone of Neogene age, above lay hard clay of
Neogene age, on them lay quaternary deposits consisting from loam, loamy sand, sand, clay
and uppermost is the thin layer of soil. Quaternary deposits can be damped by ground water.
Vertical scale in figures in 25 times stretches concerning horizontal scale.
We can know about behavior of layers within city’s territory from map of top bedrocksurface (fig. 1.5) and map of top hard clay surface (fig. 1.6).

Fig. 1.5. Map of top bedrock surface (depth from ground surface)6Fig. 1.6. Map of hard clay surface (thickness of quaternary deposits)
The map of water level (fig. 1.7) gives one more boundary of layers – between dry anddamped quaternary deposits.

Fig. 1.7. Map of water level

7

The belonging to this or that geotechnical zone defines a degree of damping quaternary
deposits. The map of geotechnic zonation is shown in fig. 1.8. We can specify three basic
zones: I - low sites of river valleys, II - terraced and watershed sites, III - steep slopes andlandslide sites.

Fig. 1.8. Map of geotechnic zonation
The spatial crossings of each of four maps have allowed to receive contours model
polygons with fixed geometrical and elastic parameters of site conditions. For example,
polygon {geotechnical zone - II / water level = 10-15 m / top of clay = 25-30 m / top of
limestone = 60-70 m} uniquely define depths of each of layers of a modeling site, and also theirelastic properties. The procedure of allocation of model polygons was carried out with use GIS(fig.1.9). Total within the limits of city more 4300 polygons were allocated, that corresponds to424 combinations of mapped parameters.

8

Fig. 1.9. Map of model polygons with fixed properties of site conditions

91.3. Elastic properties of model
The basic parameters determining elastic properties, are density and velocity of waves
in layers. We have more than 1000 boreholes with measurements of density and 118 boreholes
with measurements of velocity. It allows to define territorial and deep changes of the specified
parameters for each layer of deposits.
After the analysis of distribution of density in layers it is possible to tell, mostsignificant is the dependence of density with depth. On its background the territorial variationsof density are insignificant. Distributions of density has large dispersion and low coefficient ofcorrelation. The steady tendency of increase of density with humidifying quaternary deposits isobserved.
As an example in a fig. 1.10 the correlations of density with depth and theirapproximation for various layers on the data seismic borehole logging is shown. Coefficient ofcorrelation for various layers changes within the limits of 0,68 - 0,77. From figure it is visible,that quaternary deposits it is statistically difficult to separate by density. Quaternary and
Neogene clay obviously differ by average meanings of density.

2.2

2.0
loam

Density, g/cm^3

loamy san
sand

1.8

clay(Q)
clay(N)loam
loamy san

1.6

sand
clay (Q)clay (N)

1.4

1.2
0

10

20

30

40

50

60

Depth, m

Fig. 1.10. Correlations of density with depth and their approximation for various layers

10The analysis of wave velocities is best for considering depending from density of layers.
In this case dependencies have more universal and stable character. They are less sensitive to a
type of layers. The correlation of velocities of S-waves with density of deposits of various
composition is represented in a fig. 1.11. Owing to large dispersion of the data, the coefficientsof correlation are insignificant and make 0,5 - 0,65 for various layers. The tendency in
distribution of the data however is clearly traced. The average meanings for various layers
differ insignificantly, that specifies an opportunity of forecasting of average velocities of Swaves on the basis of the generalized dependence from density of various layers.

600

500

loam
400

loamy sanVelocity, m/сsandclay(Q)
clay(N)300

loam
loamy san
sand

200

clay(Q)
clay(N)

100

0
1.4

1.5

1.6

1.7

1.8

1.9

2.0

2.1

2.2

2.3

Density, g/сm^3

Fig. 1.11. Correlation’s of velocity of S-waves with density and their approximationfor various layers
Following the specified principles of modeling and knowledge of geometry and elastic
properties of layers in territory of Kishinev, as geophysical model for cities we used a 5-layers
medium. It is shown in the table 1 with the indication of range for properties in layers.

11Table 1
Type

Age Thickness Density Velocity

Soil

Q4

0.5

Dry deposits

Q1-4

0-20

1.52-1.78 140-230

Humid deposits Q1-4

0-22

1.71-2.03 200-350

Clay

N1

0-200

1.86-2.17 260-450

Limestone

N1

1.5

2.45

120

1300

Layers 2 - 4 have not only variable thickness, but also variable elastic properties
dependent from depth. Depending from local conditions any of these layers can be absent insome sites.
Thus, it is possible to consider creation of model completed. It has the fixed geometricalparameters (fig. 1.9) and certain elastic properties for various layers.

121.4. Comparison of amplitude-frequency characteristics of modeling and realsites
For definition of similarity degree of amplitude-frequency characteristics of modelingand real sites we shall consider some examples. In a fig. 1.12-1.15 are given pair characteristics
of four real sites and appropriate by them modeling. The depths of real bedrock are equal
accordingly 19, 40, 55 and 111 meters.
Vs, м/с
0

500

1000

9
1500

8

0

7
6
Усиление

Глубина, м

5

10

5

1549
I/13(0)-2

4
3

15

2
1

20

0
0

25

5

10

15

f, Гц

Fig. 1.12. Comparison of the characteristics of sites: real borehole 1549 and modelingfor this area I/13 (0) -2.

Vs, м/с
0

500

1000

8
1500
7

0

6

20

30

40

Усиление

Глубина, м

10

5
1554

4

III/13(5)-22

3
2
1
0

50

0

5

10

15

f, Гц

Fig. 1.13. Comparison of the characteristics of sites: real borehole 1554 and modelingfor this area III/13(5)-22.

13

Vs, м/с
0

500

1000

9
1500

8

0

7
10
Усиление

6Глубина, м

20
30

5

1531
II/23(5)-27

4
3

40

2

50

1

60

0
0

70

5

10

15

f, Гц

Fig. 1.14. Comparison of the characteristics of sites: real borehole 1531 and modelingfor this area II/23(5)-27.

Vs, м/с
0
10
20
30
40
50
60
70
80
90
100
110
120
130

500

1000

8
1500
7
6
Усиление

Глубина, м

0

5
1503

4

III/40(22)-80

3
2
1
0
0

5

10

15

f, Гц

Fig. 1.15. Comparison of the characteristics of sites: real borehole 1503 and modelingfor this area III/40(22)-80.
The observable divergences entirely are connected to difference in geometrical andelastic properties of model and real site. The model operates with average geometrical andelastic properties, real site – local properties.
The comparison of the characteristics of real and modeling sites shows their closeenough similarity and allows to use such modeling for the further analysis.

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1.5. Comparison of modeling characteristics and H/V ratio of microtremors
spectraAs a result of the spectral analysis of records of microtremors in different areas of city
the spectra of horizontal and vertical oscillations were received. In themselves spectra of
microtremors already allow to define the predominant periods of sites oscillations. From thetheory of a method also it is known, that the ratio of spectra H/V with realization of someconditions can express amplitude-frequency characteristic of a site.
In a fig. 1.16-1.19 the examples not bad similarity modeling characteristics and H/V ofspectra are shown.

5.0Усиление

4.0
3-10

3.0

I/13(10)-2
2.0

1.0

0.0
0

2

4

6

8

10

f, Гц

Fig. 1.16. H/V ratio p.3-10 and modeling characteristic I/13(10)-2.

5.0Усиление

4.0
2-18

3.0

I/13(12)-22
2.0
1.0
0.0
0

2

4

6

8

10

f, Гц

Fig. 1.17. H/V ratio p. 2-18 and modeling characteristic I/13(12)-22.

15

4.0

Усиление

3.0
5-4
2.0

II/13(10)-37

1.0

0.0
0

2

4

6

8

10

f, Гц

Fig. 1.18. H/V ratio p. 5-4 and modeling characteristic II/13(10)-37.

4.0Усиление

3.0
1-8
III/8(0)-62

2.0

1.0

0.0
0

2

4

6

8

10

f, Гц

Fig. 1.19. H/V ratio p. 1-8 and modeling characteristic III/8(0)-62.

16

1.6. Amplification properties of sites
After modeling local sites the amplitude-frequency characteristics were calculated. On
the basis of the characteristics the average amplifications of sites were determined. In otherwords, for all city territory the map of average amplification was received. The fragment of thismap for the central part of city is given in a fig. 1.20. In limits of city the peak amplification
has range 1.6-4.7, on the shown fragment of a map – from 2.0 to 4.7.

Fig. 1.20. Modeling amplification (Kishinev, Center)

For check of correctness of modeling of amplifications we compare a map of modeling
amplification with a map of damage buildings in central part of the city at earthquake 30.08.86(fig. 1.21). The given comparison is shown in a fig. 1.22 as a field of correlation of a damage
degree and modeling amplification of sites.

17

Fig. 1.21. Map of damages (Kishinev, Center, 30/08/86)

y = 0.4268x + 0.1316
R2 = 0.3635
3.0

d_av

2.0

1.0

0.0
2.0

3.0

4.0

5.0

A

Fig. 1.22. Correlation of a damage degree and modeling amplification18

It is necessary to note that the data of damages differ very large dispersion. Owing towhat the correlation them with any other parameters, as a rule, is low. In our case at small
coefficient of correlation (r=0.6), the linear tendency of increase of damage degrees withamplification factor of sites is traced.
Having transformed amplification in increment of intensity concerning the chosenreference site, we shall receive usual correlation of intensity and damage degree (fig. 1.23). The
specified transformation is carried out with the formula: ∆ I = 3.3 lg (Ai / Ao), where Ao amplification on a reference site.
y = 1.0769x + 1.1846
R2 = 0.3802

3.0

d_av

2.0

1.0

0.0
-0.5

0.0

0.5

1.0

∆Ι

Fig. 1.23. Correlation of a damage degree and modeling increment of intensity
Main in this diagram, that a ratio ∆d /∆I ≈ 1. Such ratio value connects a degree ofdamage with intensity in our region. It speaks about a correctness of the created model of sites,
its ability through amplification correctly to predict possible damages of buildings.

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1.7. Resonance properties of sites
The resonance phenomena are inherent for high buildings at closeness of the own periodsof a site and building. In practice resonant effects are expressed as additional forces and damages
received by buildings. In conditions of Kishinev the main border of layers capable to createstrong enough resonant effects is the top of limestone. In amplitude-frequency characteristics theresonant period from this border occurs by the first low-frequency maximum.
In a fig. 1.24 the correlation of the site periods with depth of bedrock is shown. The
periods of sites were calculated with the formula Тs = 4Н / Vs . In correlation the data all 118
seismic borehole logging are used. The received high degree of correlation allows with highaccuracy to use this dependence for definition of the resonant periods of sites.
y = 0.0234x0.8214
R2 = 0.9384
2.0
1.8
1.6
1.4

T_s

1.2
T_s=f(H)

1.0

Regression

0.8
0.6
0.4
0.2
0.0
0

50

100

150

200

H, m

Fig. 1.24. Correlation of the sites periods with depth of bedrock
The analysis of resonance effects can be carried out in territory with regularity built up by
high buildings (for example, Botanica area). For this purpose it is necessary to compare damagesof high buildings with ratio of the periods of buildings and sites. 164 buildings of height 8 andmore floors participated in calculations. The analysis has shown, that search of theoretical curve,
approximating experimental data optimum to do as polynomial n-power from |ln (Tb / Ts)|:dR = P {|ln(Tb / Ts)|}The initial data of damage degrees were grouped depending value |ln (Tb / Ts)| with aninterval of averaging 0,2. Thus in each interval of grouping got from 15 up to 39 buildings. The

20

simple and reliable result (r=0.99) can be received from the fourth polynomial power. The
equation looks like:d = -2.0123x4 + 6.0164x3 - 4.5847x2 - 0.7644x + 2.2085 ,where x = |ln (Tb / Ts) |. The specified dependence of damages from ratio building and site
periods is shown in a fig. 1.25.

2.4
2.2
2.0
1.8

d

1.6
1.4
1.2
1.0
0.8
0.6
0.0

0.2

0.4

0.6

0.8

1.0

1.2

1.4

|ln(Тb/Тs)|Fig. 1.25. Dependence of resonant damages from ratio of the building and site periods.
If on х-axis to not use absolute value, the general view of a resonant curve of damage
amplification can be received. It is presented in a fig. 1.26 and has typical bell-shape.

2.4
2.2
2.0
1.8

d

1.6
1.4
1.2
1.0
0.8
0.6
-1.5

-1.0

-0.5

0.0

0.5

1.0

1.5

ln(Тb/Тs)Fig.1.26. General view of a resonant curve of amplification of damages.

21

Now it is interesting to look, what becomes with an initial field of damages in Botanica
area, if from him to subtract resonant effects at high buildings? Or, in other words, what could bea map of damages with absence of additional forces connected to a resonance? The answer tothis question can be received from comparison of a fig. 1.27 and 1.28.

Fig.1.27. Map of buildings damages (Kishinev, Botanica, 30.08.86).

Fig.1.28. Map of buildings damages with the removed resonance effect(Kishinev, Botanica, 30.08.86).

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Conclusion
In conclusion it is possible to tell, that all results of modeling were used for creation of a
final map of seismic microzonation. The amplification of sites has given a basis for allocation ofzones of various intensity, and the analysis of resonant properties of sites has allowed to add on amap of microzonation isoline of the resonant periods. The map of seismic microzonation isshown in a fig. 1.29.

Fig. 1.29. Map of seismic microzonation

Literature
1. Ratnikova L. Methods of calculation of seismic waves in thin-layer medium. М., Science,
1973, 124 p.
2. Y. Nakamura. (1989). A method for dynamic characteristics estimation of subsurface using
microtremor on the ground surface. QR of RTRI, vol. 30, No 1, pp.25-33.
3. Shebalin N. Distribution of damage degrees of buildings and use it for an estimation
intensity. In book: A seismic scale and methods of measurement of seismic intensity. М.,
Science, 1975, p. 253-266.

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2. STUDY TRIPS
2.1. Study trip to Kochi
The trip to Kochi (13-14/09/2004) was undertaken with the purpose to see real
microtremors measurements, both single point, and array. The microtremors measurements werecarried out by a team from Tokyo Soil Research Co. under the direction of the Dr. Fukumoto.
We observed huddle test and measurements of small array microtremors.

Huddle test.

Microtremors measurement.

24

Processing of measurements.
Unfortunately weather conditions have prevented (was a strong typhoon) to execute forus the planned program fully.

2.2. Study trip to Fukuoka, Kyushu University
The travel in Kyushu University (4-8/10/2004) was undertaken specially for meeting with
Prof. Kawase. During four days we had with him intensive conversations about seismologicalproblems interesting for us.
In the beginning Prof. Kawase has told about his the interests in seismology. These
interests are extraordinary wide: from earthquake source mechanism up to local site conditions.
Later he has presented some of recent works concerning an estimation strong ground motion bymodeling scenario of earthquakes in Kyushu area, site effects on strong ground motion andothers.
Then I have presented my work about modeling local site conditions for the purposes ofseismic microzonation. The discussion was long and useful. Prof. Kawase was interested in finedetails. On behalf of the Prof. Kawase I have found the attentive and interested interlocutor.
Great thanks to him therefor.

25

2.3. Study trip to Hokkaido
During travel to Hokkaido (25-29/10/2004) we had an opportunity to visit some scientificcenters and unique objects representing interest from the point of view of seismology andearthquake-resistant design.
Usu Volcano Observatory. Have heard the information about work of station formonitoring of Usu volcano activity. We also had an opportunity to observe a new crater of Usu
volcano and damaged area by eruption in 1977.

Volcano Observatory.

Rupture zone.

26

New crater of Usu volcano.

Hokkaido Northern Regional Building Research Institute. The general information
about activity of Institute was heard. We also were acquainted with the equipment and work ofsome laboratories of Institute, such as: Building Materials, Structural Testing, Seismic
Resistance, Fire Testing, Sound Insulation Testing, Durability Testing, Cement and Aggregate
Testing, Outdoor Environment Simulator, Wind and Snow Environment Simulator.

Building Research Institute.

27

Air and Water Tightness Testing Equipment.

3D Vibrating platform.

28

Hokkaido University. Institute of Seismology & Volcanology. We were acquainted
with work of laboratory of seismology. Have heard some lectures of Institute collaboratorsconnected with problems of allocation of signals in seismology and system of observation andthe warning of a tsunami.

In laboratory of seismology.

Lecture about a tsunami.

29

Headquarter of Nozai Kogyo Co.,Ltd. We have learned about activity of the company
on manufacture of ceramic products for the purposes of construction, have looked samples of
production. After we have visited Nopporo Ceramic Factory, where directly have seen process ofmanufacture of ceramic products from clay.

Story about activity of the Company.

Samples of production of the Company.

30

Ceramic factory, production lines.

Chitose Shimin Hospital. The authors of the project acquainted us with a design of thisunusual building. The building stands on special LRB (Lead Rubber Bearing) and RB (Rubber
Bearing) amortization bearings. In result it is completely unreceptive to external influences.
During earthquakes the building goes under its laws.

Rubber Bearing.

31

Rubber bearing.

Kushiro Government Building. Have got acquainted with a design of this building
standing on three kinds of shock-absorbers: rubber bearing, lead damper, steel damper. In abuilding the equipment of strong motion is established. As has shown Tokachi earthquake, isachieved reduction acceleration in some times, and high frequencies cut off absolutely. Later
have looked the equipment Meteorological Observatory and work of the center of processing
meteorological data, which are taking place in the same building.

Rubber bearing and lead damper.

32

Steel damper.

Center of processing meteorological data.

33

2.4. Study trip to Kobe
Task of this travel (15-16/11/2004) was visiting Nojima Fault Preservation, the Great
Hanshin-Awaji Earthquake Museum and EDM (Earthquake Disaster Mitigation ResearchCenter).

Nojima Fault Preservation.

The Great Hanshin-Awaji Earthquake Museum.

34

In EDM we had meeting with Dr. Nelson Pulido. During which he has told about theworks on estimation strong ground motion based on source modeling. During lecture Dr. Pulido
told also two concrete works about estimation of strong motion: “Near-fault strong motion
complexity of the Tottori earthquake (Japan) from a broadband source asperity model” and“Strong ground motion estimation in the Sea of Marmara region (Turkey) based on scenario
earthquake”.

Meeting with Dr. Pulido.

2.5. Study trip to Yokohama, Kanagawa University
The purpose of trip (22/11-3/12/2004) - study of a seismic microzonation method in
Kanagawa University. From the Japanese part the curator of our activity at Kanagawa University
was the Prof. Enomoto. He has acquainted us with the approaches used by him during seismic
microzonation of Caracas city (Venezuela), about application of microtremors measurements torisk assessment for buildings in Caracas, about the experience of work on microzonation ofGranada (Spain).
During 25-27/11 we had trip together with the Prof. Enomoto in epicentral zone recent
strong Niigata earthquakes. The purpose of trip was the microtremors measurement in threetowns, injured of earthquakes: Nagaoka, Ojiya, and Kawaguchi. In passing we had an
opportunity to look consequences of earthquakes.

35

Kanagawa University.

Nagaoka, microtremors measurement.

36

Ojiya, microtremors measurement.

Nagaoka, destructions at school.

37

Nagaoka, landslide.

Ojiya, liquefaction of soils.

38

Kawaguchi, destruction zone.
On returning in Yokohama the processing of records was made, the Fourier spectra andH/V ratio are calculated. At the request of the Prof. Enomoto the presentation of my work on
seismic microzonation of Kishinev city before the personnel of laboratory and students of theProf. Enomoto was made.

Points of microtremors measurements.

39

Example of records microtremors in a point “а2” (Ojiya).

Fourier spectra and H/V ratio for point “а2” (Ojiya).

40

3. LECTURE COURSE IN BRI, IISEE AND OTHER ACTIVITY INTSUKUBA
During stay in Tsukuba we heard some lectures from the staff of BRI, IISEE Institutes
Dr. Kayama and Senior Eng. Kashima. In them such questions as were mentioned:•

theoretical bases of application of a microtremors method for study of local sites andbuildings,•

classification and characteristics microtremors,•

the equipment for measurement of microtremors,•features of Fourier transformations of a long time series, smoothing of spectra,•site conditions near BRI Institute,•strong earthquake motion observation in Japan, strong motion observation of BRI,•

dynamic behavior of 9-story base-isolated building (Kushiro Government Building) during
the 2003 Tokachi earthquake, and others.
Besides we operatively and regularly received from them the seismological information,interesting for us, on the earthquakes, which have occurred during our visit, which was much.
Also were in Tsukuba, we had an opportunity to make excursion visit in National ResearchInstitute for Earth Science and Disaster Prevention and to take part in a symposium “The 50th
Anniversary of Strong-Motion Earthquake Observation in Japan”.

41

GRATITUDE
Let to express heartfelt gratitude to Management and staff BRI, IISEE, hospitably
accepting us during long time, and in particular Kayama-san and Kashima-san, with who direct
we had deal each day. They helped us to decide any arising scientific questions.
I want to express gratitude to Professors Kawase and Enamoto hospitably accepting mein the laboratories and generous shared by their knowledges and experiences.
Let to express thanks to all personnel TBIC, for hospitality and kindliness, and especially
Sakamoto-san, Hagiwara-san, Kubota-san and Iizuka-san, who helped us to overcome living,transport and other problems.

42