STUDY OF RAPID BROADBAND MOMENTMAGNITUDE DETERMINATION FOR TSUNAMIEARLY WARNING SYSTEM IN MALAYSIA
Zamuna ZAINAL∗
MEE08176

Supervisor: Bunichiro SHIBAZAKI∗∗

ABSTRACT
We studied several methods to determine the moment magnitude, focusing on broadband P wave
moment magnitude for the purpose of tsunami early warning system in Malaysia. We determined Mwpk
based on the method by Kanjo et al. (2006). We also determined Mwp based on the original method of
Tsuboi et al. (1999) for comparison. Next we determined Mwpd’ using the duration-amplitude procedurethat was simplified from the original method by Lomax and Michelini (2008). Finally, we performed
the moment tensor inversion using the program coded by Yagi to obtain Mw. We applied all thesemethods on 20 shallow earthquakes’ data inside the region of 30°N – 15°S and 85°E – 150°E which
occurred from 2005 to 2008 and MwCMT ≥ 6.0 plus one supplemental data of the December 26, 2004
Sumatra-Andaman earthquake. Then we compared our results with the moment magnitude from the
Global CMT catalog (MwCMT).
From the analysis, we found that for larger events (Mw > 8.0), Mwpk showed good
estimation while Mwp results showed underestimation. On the other hand, for smaller events, Mwpk
showed overestimation while Mwp results showed good estimation. However, in general, both Mwpk and
Mwp estimates correlate well with MwCMT. Mwpd’ estimates produced very good results with large events.
For Mw determination using moment tensor inversion method, the results were in good agreement with
MwCMT although we found underestimations for tsunami earthquakes and great earthquakes such as theJuly 17, 2006 and December 26, 2004 events. All in all, this study has provided the base ground of
improving the tsunami early warning system in Malaysia.
Keywords: Tsunami, Mwp, Mwpd, Broadband P wave Moment Magnitude
1. INTRODUCTION
Malaysia is not an earthquake-prone country. However, due do its location which is near seismically
active plate boundaries, the country is susceptible to seismic risks and has been affected by tremors
from large earthquakes which occurred at these plate boundaries. The mega-thrust earthquake ofDecember 26, 2004 generated a very large tsunami that inundated 13 countries in the Indian Ocean
region including Malaysia. Since that time, the Malaysian National Tsunami Early Warning System(MNTEWS) has been implemented to provide tsunami early warning to the country. The MNTEWS is
currently using the Antelope system as its main seismic processing system. The system uses the bodywave magnitude scale, mb, for magnitude calculation. We know that mb has saturation effect at around
6.2 and above (Stein and Wysession, 2003). Therefore, it is not suitable for estimating the size of large
earthquakes. On the other hand, the moment magnitude scale gives a more accurate estimate formagnitude of large earthquakes. From the viewpoint of tsunami early warning system, the detection of
a tsunamigenic earthquake and estimating its size at the earliest stage is indispensable. Therefore, this∗

Malaysian Meteorological Department, Malaysia.
International Institute of Seismology and Earthquake Engineering, Building Research Institute, Japan.

∗∗

1study is being carried out to facilitate the process of upgrading the tsunami early warning system in
Malaysia by analyzing broadband seismic data using several techniques of P wave moment magnitude
determination.

2. DATA ACQUISITION
We had chosen 20 earthquakes(Mw ≥ 6.0) with hypocenter depths
shallower than 100 km which
occurred from the year 2005 –2008 inside the region of 30°N –15°S and 85°E – 150°E andretrieved the waveform data fromthe Data Management Center oftheIncorporated
Research
Institution
for
Seismology(IRIS-DMC) via internet. We also
supplemented the data with
December
26,
2004
Sumatra-Andaman
Earthquake.
We retrieved only BHZ channel
data from stations with the
maximum distance of 85 degrees
from the event’s epicenter.

Figure 1. Location of analyzed events. The focal
mechanism plot downloaded from Global CMT catalog
search (http://www.globalcmt.org/CMTsearch.html)

3. THEORY AND METHODOLOGY
3.1 Determination of broadband P wave moment magnitude, Mwpk
Following Tsuboi et al. (1995, 1999), we determined the moment magnitude using the verticalcomponent of broadband P wave seismograms (Mwp). The scalar seismic moment, M0, for each station
is obtained from the peak of maximum amplitude value of the integrated displacement of P wave train,using the following equation (Tsuboi et al., 1995):

M = max0( ∫ u (x , t)dt )4πρα r
3

s

r

(1)

where us (xr, t) is the vertical component of far-field P wave displacement at station xr, ρ and α are themean density and P wave velocity along the propagation path, respectively, and r is the epicentral
distance. The moment magnitude, Mw, is then obtained fromM w = (log10 M 0 − 9.1)/1.5(2)(Kanamori, 1977) without a correction for radiation pattern. In equation (3), 0.2 is added to the above
equation to compensate for radiation pattern as explained by Tsuboi et al., (1995) and obtained the
Mwp.
M wp = M w + 0.2(3)2

Kanjo et al. (2006) further modified the method by using a distance-dependent apparent P
wave velocity (α = 0.16∆ + 7.9 km/sec) derived from a fit to the apparent P wave velocity from the
IASP91 earth model instead of a constant apparent P wave velocity (α = 7.9 km/sec) as used by
Tsuboi et al. (1995, 1999). In this study, we used both of these values to compare the results fromeach other on our data. We denoted our results as Mwpk to refer to the application of Kanjo et al.
(2006)’s method. We analyzed the portion of 130 seconds of the seismogram beginning from 10
seconds before the initial P wave arrival time. Then we calculated the seismic moment and Mwp basedon equations (1), (2), and (3). The moment magnitude estimate for each event was then obtained byaveraging the moment magnitudes for all stations of each event.

3.2 Determination of P wave moment magnitude using duration-amplitude procedure, Mwpd’
The duration-amplitude procedure by Lomax and Michelini (2008) determines apparent source
durations, T0, from high-frequency broadband P wave seismograms, and estimate moments throughintegration of displacement records over the interval tp to tp + T0, where tp is the P-arrival time. In thisstudy, we simplified this method to determine the apparent source duration, Td, and calculate theduration-amplitude magnitude, Mwpd’.
First, we obtained the vertical component of broadband seismograms from each station andconverted it to high-frequency records using 1 – 2 Hz band-pass filtering. After performing theenvelope and smoothing function, we measured the set of time delays after the P arrival time in which
the envelope function lastly dropped below 25 percent (T25) of its peak value (Hara, 2007a,b). Then,
we calculated the apparent source duration, Td, with
Td = T 25 − TP(4)where TP is the P wave arrival time. In order to prevent the inclusion of S wave phase in the data set,
Td < TS – TP. We then obtained the average Td for all stations to get the Td estimates for the event.
Next we calculated the seismic moment using the following equation,t P + T0t P + T0
M d0 = kC M max 
u + ( t )dt ,u − ( t ) dt 
t
t
P
P



∫

∫

(5)

where k is a constant included to compensate for any unknown errors and biases in the terms of CM
and in the correction of u(t) for attenuation and geometrical spreading. CM is a constant that depends
on the density and P wave speed at the source and station, and also corrections for radiation pattern
and free-surface amplifications. For simplicity reason, we assumed that CM and the corrections were
physically exact, thus k = 1, and the term CM is defined by CM = 4πρα3r, where α = 0.16∆ + 7.9
km/sec. The moment magnitude can then be calculated based on equation (2) as follows,()

M wpd ' = log10 M d0 − 9.1 / 1.5(6)

We evaluated the seismic moment for each station using vertical component seismogramswith the following procedure: (1) Cut each seismogram from 10 sec before the P-arrival to theP-arrival time plus the source duration, Td, or 10 sec before the S arrival, whichever is earlier, toobtain P wave seismograms. (2) Integrate the P wave velocity seismogram to obtain the displacement
seismogram. (3) Integrate the displacement seismogram separately over u+(t) and |u-(t)| and choose
the maximum of these two integrals to calculate the moment estimate. (4) Apply equation (5) and (6)to the seismogram to calculate the M0 and Mwpd’ estimate.

3.3 Determination of moment magnitude, Mw, using moment tensor inversion method

3

The general expression of a vertical component of observed seismic waveform at station j is as inequation (7).
5

u j (t) =∑ ∫ dτ ∫∫∫ G (t − τ , x, y, z)M (τ , x, y, z)dV + e
V

q =1

jq

q

(7)

0

where V is the source space, Gjq is the complete Green’s function, Mq is elementary moment density
tensor and e0 is observation error. Equation (7) can also be written in vector form as the following:(8)d j = G (T ( t ), x c , y c , z c ) j m + e j

where d is the N-dimensional data, G is a N x 5 coefficient matrix, m is a five-dimensional model
parameter vector and e is the error vector. By using the least-square method, equation (8) can besolved, provided that the observation waveform (d) and convolution Green’s function with source
time function (G) are known. This method requires the assumption of the location of hypocenter andthe information of the duration and shape of the source time function. The grid search method is thenused to determine these parameters.
In this study, we used prem-modify-model velocity structure to find the moment tensor
solution. We calculated the Green’s function and body wave inversion using the program coded by
Yagi. In his program, we will try to find the best fit between the observed waveform and theoretical
waveform and determine the best depth and source duration time with minimum variance.

4. RESULTS
4.1 Determination of broadband P wave moment magnitude, Mwpk
We applied this method using two values of apparent P wave velocity, which are α = 0.16∆ + 7.9
km/sec as proposed by Kanjo et al. (2006) and α = 7.9 km/sec as in the original method by Tsuboi etal. (1995, 1999) to determine Mwpk and Mwp, respectively. In general, the Mwpk obtained correlates wellwith MwCMT although most of the events with MwCMT < 8.0 are overestimated in this study. The resultsof the Mwp obtained are in better agreement with MwCMT for the events that are overestimated by Mwpk.
However, Mwp underestimated the MwCMT for larger events. The comparison between the results with
MwCMT is shown in Figure 2. In general, the Mwpk and Mwp obtained are in good agreement with MwCMT
and consistent with the overall result as obtained by Kanjo et al. (2006). Figure 3 shows the average
Mwpk and Mwp deficits for each event plotted as a function of MwCMT.. The trend shown in Figure 3 isconsistent with the results of Whitmore et al. (2002) in which there is a decreasing deficit withincreasing MwCMT.. From this result, we can see that by using α = 0.16∆ + 7.9 km/sec, we candetermine the magnitude for larger earthquakes with better estimate.
0.8

Mwpk and Mwp (this study) deficit

Mwpk and Mwp (this study)

9.5

0.6

9.0
8.5

0.4

8.0

0.2

7.5

0.0

7.0

5.5

6.0

6.5

7.0

7.5

8.0

8.5

9.0

9.5

-0.2

6.5

-0.4

6.0

-0.6

5.5
5.5

6.0

6.5

7.0

7.5

MwCMT

8.0

8.5

9.0

9.5

-0.8

Figure 2. Comparison of Mwpk and Mwp (thisstudy) with MwCMT. (Mwpk: open square, Mwp:
solid triangle)

MwCMT

Figure 3. Magnitude deficit (Magnitude average(this study) - MwCMT) plotted as a function of
MwCMT.. (Mwpk: open square, Mwp: solid triangle)

44.2 Determination of P wave moment magnitude using duration-amplitude procedure, Mwpd’

9.5

9.5

9.0

9

Mw (this study)

Mwpd’ (this study)

For this method, we use a simplified approach to determine the apparent source duration, Td, and thenuse the measured duration to obtain Mwpd’. From Figure 4, we can see that the Mwpd’ obtained forlarge events (MwCMT > 8.5) fits perfectly with MwCMT but gradually becomes overestimated as the
MwCMT decreases. The trend of this result is quite similar to the result of the previous method.
However, this method gives better estimate with larger earthquakes compared with the previous
method. This means that by considering the apparent source duration carefully, we can determine thesize of large earthquakes with better estimate.

8.5

8.5
8.0

8

7.5

7.5
7.0

7

6.5

6.5

6.0

6

5.5

5.5
5.5

6.0

6.5

7.0

7.5
8.0
MwCMT

8.5

9.0

9.5

5.5

Figure 4. Comparison of Mwpd’ (this study)
with MwCMT.

6.0

6.5

7.0

7.5

MwCMT

8.0

8.5

9.0

9.5

Figure 5. Comparison of Mw (this study)
with MwCMT.

4.3 Determination of moment magnitude, Mw, using moment tensor inversion method
The results of Mw determination and the example output of the moment tensor inversion program areshown in Figures 5 and 6, respectively. We can see that the Mw obtained from this study correlates
very well with MwCMT. Magnitude difference between them is in the range of -0.4 to 0.3. However, we
can also see that the differences between July 17, 2006 tsunami earthquake and December 26, 2004
mega-thrust earthquake are relatively larger than the others (-0.5 and -0.7, respectively).
(a)

(b)

(c)

(d)

Figure 6. Example of output result from moment tensor inversion
program by Yagi. The upper part shows (a) the focal mechanism,(b) the source time function and (c) the source parameters. The
lower part (d) shows the waveform fitting. Red and black lines
indicate theoretical and observational waveforms, respectively.

55. CONCLUSIONS
From our analysis, we found that Mwpk is overestimated for smaller events (Mw < 8.0), while Mwp isunderestimated for larger events (Mw > 8.0). However, in general, both Mwpk and Mwp estimatescorrelate well with MwCMT. On the other hand, Mwpd’ estimate produced very good results with large
events due to the usage of duration-amplitude procedure. For determination using moment tensor
inversion method, the obtained moment magnitudes were in good agreement with MwCMT. However,
we could not acquire a good estimate for tsunami earthquakes and great earthquakes such as the July17, 2006 and December 26, 2004 events. This is because the moment tensor inversion program
determines Mw using body wave signals while MwCMT is determined by using long period surface
waves. The analysis using short period body waves cannot determine the size of very large
earthquakes.

6. ACTION PLAN
In order to use the broadband P wave moment magnitude scale into the current seismic processing
system in Malaysian Meteorological Department (MMD), we need to integrate the calculation
program into the system. However, this needs further discussion between MMD and the systemdeveloper, Boulder Real Time Technologies, Inc. (BRTT). Nevertheless, this study has provided thebase ground of improving the tsunami early warning system in this country. It is important becausefrom the aspect of tsunami hazard assessment, a rapid and accurate determination of an earthquake
size, together with the other source parameters, is essential to classify whether the earthquake istsunamigenic or not. In consequence, a tsunami early warning or other appropriate information can bedisseminated. Therefore, on the basis of this study, I plan to work together with the department and thesystem developer to construct a way of implementing the broadband P wave moment magnitude
determination method in our tsunami early warning system. Other than that, I also plan to further
studying other recent methods for magnitude determination in the future for further understanding theearthquake source process.

ACKNOWLEDGEMENTMy heartfelt appreciation goes to Prof. Yuji Yagi of University of Tsukuba for kindly providing mewith his moment tensor analysis program.

REFERENCES
Hara, T., 2007a, Earth Planets Space, 59, 227-231
Hara, T., 2007b, Earth Planets Space, 59, 561-565
Kanamori, H., 1977, J. Geophys. Res., 82, 2981-2987
Kanjo, K., Furudate, T., Tsuboi, S., 2006, Earth Planets Space, 58, 121-126
Lomax, A. and Michelini, A., 2008, Geophys. J. Int., 176, 200-214
Stein, S. and Wysession, M., 2003, Blackwell Publishing, UK
Tsuboi, S., Abe, K., Takano, K., and Yamanaka, Y., 1995, Bull. Seis. Soc. Am., 85, 2, 606-613
Tsuboi, S., Whitmore, P. M., and Sokolowski, T. J., 1999, Bull. Seis. Soc. Am., 89, 5, 1345-1351
Whitmore, P. M., Tsuboi, S., Hirshorn, B., and Sokolowski, T. J., 2002, Science of Tsunami
Hazards, 20, 4, 187-192
Yagi, Y., 2008 – 2009, Lecture Note, IISEE/BRI

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