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EARTHQUAKE LOCATIONS AND THREE-DIMENSIONAL
SEISMIC STRUCTURE OF SOUTHERN PERU
by
Paul S. Cunningham
S.B., Massachusetts Institute of Technology
(1984)
SUBMITTED TO THE DEPARTMENT OF EARTH, ATMOSPHERIC, AND
PLANETARY SCIENCES IN PARTIAL FULFILLMENT OF THE
REQUIREMENTS FOR THE DEGREE OF
MASTER OF SCIENCE
in
Earth and Planetary Science
at the
MASSACHUSETTS INSTITUTE OF TECHNOLOGY
May, 1984
* Massachusetts Institute of Technology 1984
........
Signature of Author .................
Department of Earth, Atmpspheric, and Planetary Sciences
May 24, 1984
Certified by ...
Steven W. Roecker
Thesis Advisor
Accepted by .......
S
LIBRARIES
Theodore R. Madden
Chairman
Departmental Committee on Graduate Students
EARTHQUAKE LOCATIONS AND THREE-DIMENSIONAL
SEISMIC STRUCTURE OF SOUTHERN PERU
by
Paul S. Cunningham
Submitted to the Department of Earth, Atmospheric, and
Planetary Sciences in partial fulfillment of the
requirements for the Degree of Master of Science in
Earth and Planetary Science
ABSTRACT
Arrival time data, acquired in southern Peru during the summer of 1981,
were used to relocated microearthquakes using three-dimensional structures
to model lateral heterogeneities of the crust and upper mantle. The results of
these relocations were very similar to the original hypocentral solutions
computed by Grange(1983), indicating that the simple fiat layered structures
which he used were reasonable approximations to the actual structure. The
tectonic characteristics of southern Peru were equally well defined with either
set of earthquake locations. The most prominent feature, the bend in the
Nazca plate as it is subducted under southern Peru, was located beneath the
northern end of the volcanic arc in the region. North of the bend, the slab is
being subducted at a shallow angle (10 -15*), while south of the bend, the slab
is descending at a steeper angle (250 -30*). These observations corroborated
the theory of Barazangi and Isacks (1976;1979) that a wedge of aesthenosphere
is required between the overridding and subducted plates, for subductionrelated volcanism to occur. It was also shown that the contorted zone of the
Nazca plate is parallel to the plate's direction of motion with respect to the
South American plate.
A subset of the well located events was then used to perform threedimensional velocity inversions in an attempt to model the seismic structure of
the region. Criteria established by Roecker (1982) to aid in the interpretation of
the inversion results were used. The features that appear from these results
are the following: First, a velocity gradient seems to exist perpendicular to the
coast. The velocities are higher in the southwest crossing the Moho under the
coast, and decrease under the Western Cordillera of the Andes and the
Altiplano. Second, the Moho at its deepest point under the Altiplano, seems to
be at a depth of about 70 km. Third, the upper mantle seems to be a region
where P and S velocities are gradually increasing with depth, with the exception
of a few P velocity anomalies between 70 and maybe as much as 130 km depth.
The average velocities for this region seem to be in the range of 7.5 to 8.0 km/s
for the P, and 3.9 to 4.6 km/s for the S. The velocities for the anomalies were
greater than 8.0 km/s and less than 7.5 km/s. Finally, an S wave low-velocity
zone is seen between 100 and 130 km depth. However, it does not seem to be as
pronounced as it was originally thought to be, when Wadati plots were made to
determine Vp to Vs ratios for different depth slices.
Thesis Supervisor: Dr. Steven W.Roecker
Title: Research Associate
-2-
ACKNOWLEDGEENTS
This thesis is dedicated to my parents and to the friends I have made
during my years at MIT, especially the brothers at the Pi and the FWFW women.
Special thanks go to Peter Molnar who aroused my interest in this project;
to Steve Roecker without whose help and guidance I would not have been able
to do this paper; and to Debby Roecker for her help in eliminating many of the
bureaucratic hurdles at MIT.
-3-
TABLE OF CONTENTS
ABSTRACT .........................
.. .. .. .. .. . .. . ..
......
.............
22.................
ACKNOWLEDGEMENTS ......................................................................................
3
.....................................................
5
.............
7
I. IN TRODU CTION ...........................................
II. THE TECTONICS OF SOUTHERN PERU ......................
12
III. SEISMIC DATA INVERSION THEORY ...................................
III.1 The Inversion Problem .....................................................................
12
111.2 The Stochastic Inverse vs. the Generalized Inverse ......................
15
111.3 Decoupling the Hypocenter and Velocity Solutions ....................
18
111.4 Obtaining Solutions and Estimating their Reliability .................
19
IV. MICROEARTHQUAKE LOCATIONS IN SOUTHERN PERU ..................................
22
IV.1 Original Hypocentral Solutions ..................................
22
IV.2 3-D Hypocentral Relocations - The Initial Model ............................
24
IV.3 3-D Hypocentral Relocations - Refining the Crustal Model ...........
26
IV.4 Final Observations .............................................................................
29
V. THREE-DIMENSIONAL VELOCITY INVERSIONS .......................................
31
V.1 Procedure and Estimated Confidence Indicators ..........................
31
V.2 Analysis of the Inversion Results ............................
34
VI. CO NCLU SIO NS .......................... .................................
BIBLIOG RAPHY .....................
...........
FIG U R E S ....................................... .....
.
........... .........................
38
......................
40
...............................
...............................................................
43
APPENDIX A .....................................................................
115
.............................
125
APPENDIX B ....................................
-4-
ICHAPTER 1
IITRODUCION
The subduction of the Nazca plate beneath the western margin of South
America, is the archtypical example of subduction of an oceanic plate beneath
a continental plate. It is the object of many studies, not only to understand
what is occurring along the western edge of South !America (the "Andean "
margin), but to gain insight into :the processes which followed this same model
in other parts of the world in past eras. Being a seismicaly active region,
information can be gathered about the tectonic deformation from the crust
down to hundreds of kilometers within the mantle. Distinctive features of the
region can be recognized, an example being the deformation of the Nazca plate
as it is subducted under southern Peru. By analyzing shallow and intermediate
depth rnicroearthquakes, the geometry of this particular feature as well as the
patterns of deformation occurring within the crust can be better understood.
Temporary seismic networks were installed in central and southern Peru
during the summers of 1980 and '1981 to record :nucroearthquakes.
The
recorded P and S arrival times were used by Grange (:1983) to study the
deformation of the crust and of the Nazca plate subducting beneath South
America.
In the study carried out by this author, only the arrival times
recorded in 1981 were used. With this data, earthquakes were'relocated using
three-dimensional
models of the crust and upper mantle.
Next, three-
dimensional velocity inversions were carried out to determine the velocity
structure of the region.
The results were then anialyzed in terms of the
tectonics and seismic characteristics of the region.
This project was carried out be faculty members and students of the
Massachusetts Institute of Technology and of the Universitd de Grenoble with
help from staff of the Instituto Geofisico del Peru and other individuals.
This paper begins with a brief overview of the tectonics of southern Peru, a
large portion of the information being based on work described in papers by
members of this project (Grange (1983), Grange et al., (1984a;1984b)).
Next, a
review of the problem of determining earthquake hypocenters and inverting for
the velocity structure is carried out in chapter 3. Chapter 4 describes the
manner
in which
initial
velocity
structures
were
determined
and
the
earthquakes relocated, along with an analysis of the seismicity patterns. The
velocity inversions and the implications of their results are described in
chapter 5.
Appendix A contains a list of 396 events considered to be well
located used in the velocity inversion. Appendix B contains the computer
printouts of the inversion runs.
-B-
CHAPTER 2
THE TECTONICS OF SOUTHERN PERU
Earthquakes that occur at intermediate and deep depths within the
subducted oceanic lithospheres define the geometry of the downgoing slabs.
These seismic zones generally outline simple, inclined planes, but often show
that the subducted lithosphere is contorted or discontinuous. For example,
profiles of different parts of the subducted portion of the Nazca plate beneath
0
*South America show that the dip of the seimic zone varies between 10 15 and
25"-300 [Swift and Carr (1974); Barazangi and Isacks (1976;1979)]. Under
northern and central Peru, and again under central Chile, the seismic zone dips
at a gentle angle (100-150 ), while under southern Peru, Bolivia and northern
°Chile the dip of the seismic zone is steeper (25
3 00
).
Barazangi and Isacks (1976;1979) made profiles perpendicular to the coast,
using data from the International Seismological Center.
They inferred the
existence of a discontinuity in the seismic zone trending northeast through
160 S, 720 W, and implied a tear in the slab (Figure 1). However, Hasegawa and
Sacks (1981), using earthquake locations based on data from a local network of
stations, pointed out that any discontinuity of the seismic zone would be small,
the prominent feature being a contortion in the slab and not a tear (Figure 2).
Corroborating this result, Grange (1983) and Grange et al. (1984a;1984b), using
microearthquake
data collected in 1980 and
1981,
showed that profiles
perpendicular to the coast had the same dips as those of Hasegawa and Sacks
(1981), gradually becoming shallower towards the northwest (Figure 3). The
focal depths of these earthquakes were as great as 250 km in the southeast but
-7-
no deeper than 130 4km in the northwest. Profiles made parallel to the coast
also showed a bend in the seismic zone with no offset of the seismic activity that
would imply a tear between the two parts of the slab (Figure 4). Morever, maps
of the earthquake epicenters at different depth intervals show a gradual
broadening of the seismic zone to the northeast for depths greater than 100 km
(Figure 5).
Grange :(1983) and Grange et al. (1984a;1984b), also showed that the
transition zone is parallel to the direction of motion of the Nazca plate relative
0
to the South American plate (approximately N80 E) and not perpendicular to
the coast as both Barazangi and Isacks (1976;1979) and Hasegawa and Sacks
(1981)
had implied.
This can be clearly seen by observing that profiles
perpendicular to the coast flatten out towards the northeast at large depths,
while profiles parallel to N800 E do not show any change in the dip of the
seismic zone for each profile (Figure 6). This feature can also be seen if
contours of the events at different depth ranges are made on a map (Figure 7).
Because of this orientation, it is not necessary for the transition zone within
the Nazca plate to migrate with respect to the South American plate.
Barazangi and Isacks (1976;1979)
pointed out the lack of Quaternary
volcanism of ,the :South American plate in areas where the Nazca plate is being
subducted at a shallow angle, and its occurrence where the subduction of the
Nazca
plate
is
at a
steeper
angle.
They
inferred
that
a wedge
of
aesthenospheric imaterial must exist between the overriding plate and the
subducted
plate
for subduction-related
volcanism
to
occur.
They also
estimated the "tear" in the Nazca plate to be about 100 km southeast of the
northernmost volcanoes. But the results of Grange et al. (1984a;1984b) show
that the bending lof the Nazca plate actually seems to occur under the northern
-8-
edge of the volcanic arc in southern Peru.
This would further support
Barazangi and Isacks's reasoning for the need of a wedge of aesthenosphere to
exist between the plates.
The locations of shallow microearthquakes within the South American plate
were divided into three belts parallel to the coast by Grange (1983), and Grange
et al. (1984b): a group offshore between the trench and the coast following the
1800 m bathymetric contour, another beneath the coast, and a third under the
Western Cordillera of the Andes. In addition, a few scattered microearthquakes
were located within the Altiplano.
Both the offshore belt of activity and the belt beneath the coast, despite
being separated by a gap, seem to be associated with the slip between the Nazca
and South American plates. The offshore group appears to occur below the
South American crust at the interface between the two plate. The group under
the coast, though, does not seem to occur at the base of the crust, but between
slabs of mantle lithosphere. The fault plane solutions for this last group do not
show simple underthrusting, but a variety of deformation styles (Figure 8).
Although each solution can be explained in terms of plate deformations, no
clear interpretation for the group as a whole could be made. No fault plane
solutions could be made for the offshore group due to the distribution of the
recording stations.
The belt of earthquakes located under the Western Cordillera is situated 60
to 100 km from the coast, and occurs in both the crust and the mantle. The
belt seems to terminate at about 160 S in the northwest direction, and in the
seismicity maps of Grange (1983), extends only as far south as 170S. However,
this does not appear to be the actual southern limit of the belt, but the result
of the elimination of poorly located events in the region.
-9-
The fault plane
solutions for some of these events show a rather unexpected deformation style.
Thrust faulting is predominant towards the northwest end of the belt, while
earthquakes towards the southeast, have large components of strike slip
faulting. For both cases, neither nodal plane for most of the events parallels
the seismic zone. However, the P axes for both types of faulting do parallel the
zone, thus suggesting some crustal shortening in the southeast-northwest
direction.
The fault plane solutions for the few events within the Altiplano indicate
mostly normal faulting. These last few events are characteristic of the present
tectonic state of the Altiplano, as described by Suarez et al. (1983) and others.
The low level of seismicity of the crust and upper mantle under the coast,
coupled with the fault plane solutions for the events under the Western
Cordillera give no indication of any active "tectonic erosion" of the leading edge
of South America. This concept of tectonic erosion has been used by a number
of authors [e.g. Plafker (1972); Rutland (1971)] to explain the exposure of
Precambrian rocks near the coast of Peru and the inland migration of
volcanism over the last 100 m.y. If such erosion of the plate does occur, it
seems to be aseismic, and any crustal thickening perpendicular to the Andes
takes place along its eastern edge [Suarez et al. (1983;1984)].
A few other points of interest were noted by Grange et al. (1984b).
First,
there is an apparent gap in seismicity in the southernmost part of the area
studied between depths of approximately 130 and 180 km (Figure 3). Since the
station networks were recording only for short periods of time during the
summers of 1980 and 1981, one cannot conclude that this gap is permanent.
But its existence does not seem to be due to poor locations. Second, there
seems to be a small decrease in the seismic activity within the steeply dipping
- 10-
zone when compared to the contortion zone. This is in agreement with the idea
that there are greater stresses and more rapidly occuring deformations within
the contorted part of the downgoing slab. The third point concerns the shallow
events under the Western Cordillera whose northern limit is close to the zone of
bending of the Nazca plate. Since this zone is actually slightly farther north,
and at a greater depth than the shallow events, one cannot directly correlate
the stresses associated with these events with the bend. But it seems entirely
plausable that these earthquakes may be related to the occurrence of active
volcanoes,
which
in turn
are
linked
to the
aesthenospheric material between the plates.
- 11 -
existence
of
a wedge
of
CHAPTER 3
SEISMIC DATA INVERSION THEORY
I.
The Inversion Problem
The inversion problem under consideration involves matching observed and
calculated travel time data by simultaneously determining the hypocentral
parameters (origin time, latitude, longitude and depth) for each event, and the
velocities of elastic waves in a three-dimensionally varying structure. We
proceed by formulating the problem in the following fashion:
A set of observed arrival times of waves'from r earthquakes recorded at s
stations can be described by
tv = tij [z,Yk)
,zT24',zY,
for i = 1,2,.....,r
2 ..--.]
(1)
and .j = 1, 2,.....,s
where z1i through z 4 i represent the hypocentral parameters and y through yk
represent the k parameters used to describe the velocity model used. For the
sake of clarity we will describe this entire set:of parameters by a vector X with n
components (n = 4r + k).
Given an initial set of model and hypocentral parameters X., we can
calculate a travel time for each hypocenter (the forward problem), and
compare it with the observed travel time. The diference between these times the travel time residual - is then minimized in a least squares sense by making
- 12-
adjustments to the initial solution. The travel time functions are nonlinear
functions of the hypocentral and model parameters, which we can estimate by a
linear system of simultaneous equations using a Taylor series expansion. The
travel time residuals can now be described by
+
=16
gos - t FtA
= At1
(2)
- tij
(3)
Here
Azl = z
-z0,
and
AtV
= tj
where the subscript o denotes values calculated using the initial set of
parameters. The variable si represents the contribution of noise and higher
order terms. Using matrix notation, (2) becomes
G&
(4)
= a+i
where G is an m z n matrix of partial derivatives, & is a "correction" vector
(= X -),
and d is a vector of travel time residuals.
The vector 4i whose
elements are the Eq, represents the error found in the data. The "correction"
2
vector is determined by minimizing id - GxI] . Thus the changes in travel time
needed to eliminate the residuals can be expressed in terms of corrections to
the initial model and hypocentral parameters to obtain a "best fit" solution.
The actual solution, AM of the least squares problem is approximated by a
generalized inverse solution, M'(Aki and Richards, 1980) through the operation
fl =
T
G
IGG)
a
(5)
However, because GTG may have small eigenvalues, a stochastic inversion is
used instead. The stochastic inverse provides a damping factor which prevents
- 13-
a solution from becoming unstable. Furthermore, this inverse rPuis only
relatively simple matrix operations, while the generalized inverse r~quies a
complete eigenvector analysis. The solution described here, a special case of
the stochastic inverse, is of the least squares variety (Franklin, 1970; Aki and
Richards, 1980):
= L(G)
(
where the stochastic inverse operator is
(7)
L = (GTG + 2-') GT
The damping term 62 is the ratio of the variance of the data to the
variance of the model,
contributions
due
to
-,
am
and I is the identity matrix. In this inversion,
eigenvectors
with
small eigenvalues
(X < t5)
are
suppressed. As discussed in the next section, although & does not satisfy (4)
exactly, it represents a smoothed version of the true model.
As shown by Lanczos (1961), any rectangular matrix can be decomposed
into three matrices:
G = UAV
(8)
where U is an m z m matrix whose columns span the data space of G, A is an m
.z n diagonal matrix containing the singular values of G, and VT is the transpose
:of an n z n matrix V whose columns span the model space of G. We can divide V
jinto two parts, V and Vo, where Vp consists of the eigenvectors with nonzero
:singular values and Vo is made up of eigenvectors with zero singular values.
-Here, p, the number of nonzero singular values found in A, is the number of
-14-
independent parameters used to determine the solution. In the same ashion,
we can divide the matrix U into two parts: U,, representing the nonzero
eigenvalues, and Uo, representing the zero eigenvalues. U, can be further
divided as shown below [U, = (Ul, U2).
We are working with an overdetermined system of m equations (m = rs), n
unknowns (n = 4r + 1) and p independent parameters. Our data space, then,
consists of p pertinent bits of data and m-p bits of excess data. Thus we can
say that part of Up, which we will call U1, spans the pertinent data space, while
the remainder of U,, call it U2 , will span the excess data space along with U0.
Schematically we have
G_
U1 U2 UO
- V
---
0V
II.
(
()
0
The Stochastic Inverse vs. the Generalized Inverse
The reason for using the stochastic inverse can be illustrated as follows.
As we noted earlier, the solution to the generalized inverse is described by (5).
We can then take the decomposition of '(8) one step further, as shown by
Lanczos (1961), where
G = UPAV
(10)
This is possible as the Uo and Vo spaces are not mapped by the operator G. By
- 15-
substituting (10) into (5), we then have
(11)
= V,' p-Upr
where
Aih- =
(12)
x-1
In the neighbourhood of any singularity, one or more small eigenvalues
mapped through (11) would produce large changes in the parameters contained,
in ih. These small eigenvalues then become a source of instability by reducing
the precision of the calculations when the inversion of large matrices are
carried out, as well as causing an amplification of the noise within the data. In
addition, this instability could cause the solution to diverge as the calculations
proceed from one iteration to another.
Because of this problem in the neighbourhood of singularities, a method
that suppresses large changes due to small eigenvalues is desirable.
stochastic inverse introduced by Franklin (1970)
The
performs this stabilizing
function for small eigenvalues. By substituting the stochastic inverse operator
(7) and the matrix decomposition (10) into the stochastic inverse solution (6)
we have
aI = Vd
Here
Upa
+ i21
Here each element of the diagonal matrix is given by
- 16-
(13)
+
Xt
As we can see, small eigenvalues, specifically those smaller than the
damping term
eigenvalues
62,
cause the changes in the parameters to decrease. As the
decrease, the changes
approach zero smoothly, instead of
approaching infinity, as in the case of the generalized inverse. This process is
illustrated in the figure below:
-
(Generalized Inverse)
Parameter
Changes
(Stochastic Inverse)
Comparison of the influence of small eigenvalues on the behavior of
parameter changes for the generalized and stochastic inverse methods.
- 17-
II.
Decoupling the Hypocenter and Velocity Solutions
As noted earlier, these inversion methods solve for the changes made to
the model and hypocentral parameters. However, by including the hypocenter
for each event four rows and columns are added on to the matrix of partial
derivatives. This leads to difficult storage and computational problems when
carrying out the calculations.
On the other hand, if perturbations to the
hypocenters are not considered - that is, the hypocenters are fixed - we are
assuming that there is no coupling between the hypocentral and the model
parameter solutions. To overcome this problem, Pavlis and Booker (1980) and
Spencer and Gubbins
(1980)
proposed methods of solving an equivalent
inversion problem in which the hypocenter parameters are separated from the
velocity parameters. With the notation of (4), this is
d = GH + B +
(14)
where H is the vector containing changes in hypocentral parameters, and V is
the vector containing the velocity changes. As before, we can decompose G into
the form of (9), where UI spans the pertinent data space of G.
elements of the
hypocenters,
Now the
residual vector, which map into U1 will determine
while
the
remaining
elements
will
determine
the
the velocity
parameters or be considered noise.
Since the system of equations is overdetermined, U 2 is assured to exist. Its
columns will be orthogonal to U1 so that if we premultiply (14) by U2, the
hypocentral solution will be detached from the velocity solution because
U
d
=: UTB
+ U2
(15)
By this method, as much data as is desired can be utilized while only a number
- 18 -
of columns and rows equal to the number of parameters being solved for is
stored.
The inclusion of S wave velocities in the solution increases the accuracy of
the earthquake location. Although increasing the number of parameters used
to describe the model, the hypocenter locations become more stable, being less
susceptible to changes in the velocity structure than when only P waves are
used [Chatelain et al. (1980)]. As stated by Roecker (1982) "the S waves appear
to rotate the Ux space of the hypocenter matrix out of the U1 space of the
velocity matrix, thereby uncoupling the solutions". If both P and S waves are
used for the locations, both also have to be used when solving for the velocity
structure. Otherwise, we would be working with different U spaces, each of
which
would
cause
different
residual components
to
project
onto
the
hypocentral solution.
If both types of waves are used simultaneously, it is reasonable to assume
that some amount of coupling may occur between the velocity parameters.
Then, it would be best if the solutions for the P and for the S wave velocities
could be decoupled in the same fashion as the hypocenter and velocity
solutions were.
This being a difficult task however, we cannot hold the S
velocities fixed, but must let them vary in the same manner as the P velocities.
IV.
Obtaining Solutions and Estimating their Reliability
To avoid nonlinearity effects when trying to obtain stable solutions, either
the partial derivatives in G must be nearly constant, or the corrections in i
must small. To avoid violating these conditions of linearity, we can vary the
- 19-
parameters in a sequential fashion. This is done by beginning the inversion
,i.e., the one with the smallest partial
with the least sensitive parameter
derivative. In this manner, with each successive step, the residuals are reduced
making subsequent corrections smaller. The sequence in which the parameters
are allowed to vary begins with the hypocentral latitude and longitude, followed
by the focal depth and origin time, phase velocities of the blocks, and the
changes
in
the
fractional
slowness
(1/velocity)
of
the
structure.
This
procedure was called a "progressive" inversion by Roecker (1982).
The confidence we have in our solutions can be measured through two
reliability estimators: the covariance matrix C, which gives us an estimate of
the standard error of the solution, and the resolution matrix R, which indicates
the degree
to which our calculated solution approximates
the true least
squares solution.
The error within the data, Ad, will produce an error Am in our solutions
which can be expressed through the covariance matrix (Aki and Richards, 1980)
as
C = <AmAmT> = adLLT
=
+ 61
vP
(16)
where au is the estimated variance of the data.
The resolution matrix is given by Mt= lih
or
R =LG
= V
(Aki Richards,+and
1980).21
(Aki and Richards, 1980).
-20-
(17)
Should any diagonal of R be zero, the corresponding parameter cannot be
resolved. If, on the other hand, R is the identity matrix, then the solution is
perfectly resolved and we have calculated the true solution (l = i).
The
manner in which one interprets R for values between zero and one is rather
subjective, but it often allows us to separate what we consider to be reliable
solutions from unreliable solutions.
- 21 -
CHAPTER 4
MICROEARTHQUAKE LOCATIONS IN SOUTHERN PERU
The data used for this paper were acquired during the summer of 1981 in
southern Peru. A temporary network of smoked paper recorders was installed
in a dense array, the stations being within or close to the Western Cordillera of
the Andes (Figure 9). In addition, data from station ARE of the World Wide
Standardized Seismograph Network (WWSSN) and two stations installed by the
Department of Terrestrial Magnetism of the Carnegie Institution in Washington
(ONG and AYE) were used.
Over 20,000 P and S arrival times from approximately 3,000 events were
read using a digitizing table.
account the uncertainties
The uncertainties of these data, taking into
of the measurements,
drifts of the recorders's
internal clocks and variations in drum rotations, were estimated to be less than
0.1 seconds for P arrival times and about 0.8 seconds for S arrivals.
I.
Original Hypocentral Solutions
Over 1200 events were initially located by Grange (1983) using the program
HYPOINVERSE [Klein (1978)] after it had been modified to include elevation
corrections. This correction was necessary since the altitude of the stations
varied from sea level to 4,900 m. A series of tests was carried out to evaluate
the quality of the locations so that the results could be discriminated between
more or less reliable locations. Further tests were made to determine whether
- 22-
or not it was valid to use flat layered structures, and to see ff any lateral
heterogeneities could be approximated by these methods. The results of the
locations and tests were described in detail by Grange (1983) and Grange et al.
(1984b),
and are
summarized here.
It was
decided
that a
reasonable
approximation of the probable structure could be made by using three different
simple layered models together. The three models corresponded roughly to the
region between the trench and the Peruvian coast, the coastal region, and the
region under the Western Cordillera and the Altiplano (Figure 10). Different
stations were assigned to each model. The criteria arrived at to determine good
locations were the following:
(1)
A minimum of eight phase arrivals, at least one being an S-wave arrival.
(2)
A root mean square value of travel time residuals (RMS) less than 0.40 sec.
for events with 20 or more arrival times (N), an RMS less than 0.35 sec. for
15 < N < 20, and an RMS less than 0.30 sec. for 8 < N < 15.
(3)
Estimated epicentral and focal depth errors of less than 10 km.
(4) Events with a maximum azimuthal
aperture without stations
(GAP)
measured from the epicenter greater than 3000, must have an epicentral
distance to the nearest station (DMIN) less than one-half the calculated
focal depth. For events with a GAP less than 3000, DMIN must be smaller
than the calculated focal depth for events deeper than 60 km, and less
than twice the calculated focal depth for events shallower than 60 km.
To minimize bias in locations introduced by erroneous choices of velocity
structure, the only events that were retained were those whose locations did
not change by more than 10 km when relocated using different velocity
structures.
592 events met these criteria, and the errors for depth and
- 23-
epicentral coordinates were estimated to be no more than 5 k
and' 7 kmn
respectively. An additional 296 events were retained, since 1mey bad stable
solutions, although they did not fulftll all the criteria above.
II.
3-D Hypocentral Relocations - The Initial Model
For the purposes of this study, the work done by Grange (1983), (described
in the previous section) provided us with a set of events with stable solutions.
These events were relocated using three-dimensional velocity models, which are
presumably a more realistic approximation of the probable structure than that
used by Grange. By relocating these events in a realistic structure, any errors
due to lateral heterogeneities would be reduced. Also, the events would be
located within a structure that could be used as an initial model for a threedimensional velocity inversion. Assuming that the relocations were reasonably
accurate, any changes of the hypocentral parameters made during the
inversion would be relatively small. This was a necessary condition to avoid
instabilities due to the nonlinearity of the inversion problem. Both the set of
events retained by Grange and a portion of the set he discarded for having
failed his reliability criteria were relocated.
The initial three-dimensional model was set up by taking a rectangular
prism, aligned parallel to the Peruvian coast, centered about 16*S, 72' W. The
dimensions of the rectangle, within which all the events are located, are 440 km
in length by 330 km in width, or approximately 40 by 30 of arc. Next, a crosssection of the layers was taken perpendicular to the Peruvian coast. Each layer
was divided up into blocks in a southwest to northeast direction. This profile
was then extended in a southeast-northwest direction, producing a three-
- 24-
dimensional structure (Figure 11). The geometry and assigned meloities,
ased
nd
eyer
on work by Grange (1983) (Figure 10), James (1971), and Ola
(1973) (Figure 12), modeled a crust that thickened from the trench towards the
Western Cordillera, and then thinned towards the Brazilian Shield. In this frst
relocation, the mantle below 70 km depth was modeled by one homogeneous
block.
Once the relocation run was completed, the first step taken to pick the
more reliably located events was to remove those events whose matrix of partial
derivatives produced small eigenvalues.
(Small eigenvalues were defined as
those whose ratio to the largest eigenvalues was less than 0.D1). Next, the
events that showed some degree of instability - that is, those whose hypocentral
parameters oscillated by large amounts from one iteration to the next - were
discarded. The limits imposed on the oscillations were on the order of 2 to 3 km
for latitude and longitude, 3 to 4 km for focal depth, and 1.0 sec for origin time.
We noted that a few events with large changes in the hypocentral parameters
required several iterations before converging.
The criteria used by Grange
(1983) was then applied, and 467 of the approximately 1,100 earthquakes
satisfied all conditions. When the RMS criterion was relaxed, an additional 109
relocated events were considered reliable. This relaxation of the rule was the
following:
(1)
For number of phases (N) less than 15, the RMS had to be less than 0.5
seconds.
(2)
For 15 < N < 20, an RMS of less than 0.6 was required.
(3)
For N > 20, the RMS could not be greater than 0.7 seconds.
-25-
Over ninety percent of the chosen relocations were amongi~tase events
determined by Grange to be more reliable. A closer comparison of the results
showed that most of the new locations tended to be slightly farther northeast
and shallower than Grange's locations, and the origin time occured about 1
second later. The changes in locations were on the average no.greater than 10
km. This appears to indicate that the data favors the parts of the model having
slower than average crustal velocities. The estimated precision of the relocated
events is approximately the same as those from Grange (1983).
Few events
located at depths greater than about 90 km satisfied all the criteria, suggesting
that it is not sufficient to model the upper mantle by using one homogeneous
block.
l.
3-D Hypocentral Relocations - Refining the Crustal Model
A second relocation was carried out, the purpose being to detect a few of
the characteristics of the crustal structure on a smaller scale (e.g., tens of
kilometers). Also, the events would then be located within a model that would
then be used as an initial solution for the three-dimensional velocity inversion.
The principal aim was to try to determine the approximate location and
shape of the Mohorovi6ic discontinuity (the Moho), across which the phase
velocities
should
increase
substantially.
Previous
studies
(for example,
Anzoleaga (1964), James (1971), Ocola et al. (1971), Ocola and Meyer (1973))
seem to agree on a Moho increasing from the coast towards the Andes.
It
appears to reach a maximum of 70±10 km under the Altiplano and then
gradually becomes shallower towards the Brazilian shield (Figure 12).
-
26-
Another important
consideration in setting up the model, was te
Based on large amplitude secondary
existence of low velocity zones (LVZ).
arrivals from refraction studies in the Altiplano, Ocola and Meyer (1972) stated
that there existed two thin LVZs within the crust.
However, since the
dimensions of these low velocity zones were too small to be resolved, they were
not included in the model. The remaining major boundary across which a
change in velocity could perhaps be modeled was the LVZ that occurs within the
mantle. According to James (1971), there .did not appear to be any significant
LVZ for shear waves in the upper 150 km of mantle beneath the continental
crust, although it seemed that both P and S velocities were somewhat low. Yet,
a major S wave LVZ was required under the oceanic crust in the area to satisfy
phase and group velocity data. He set the upper boundary of this LVZ between
50 and 60 km depth, and the lower boundary at a depth greater than 200 km.
To determine whether the existence of a LVZ could be resolved, a series of
Wadati plots was made to calculate the Vp to Vs ratio for different depth slices
(Figure 13).
This was done by ploting Vp minus Vs arrival times versus Vp
arrivals. The slope of this graph minus one is equal to the average Vp to Vs
ratio down to that depth slice. Since the ray paths for the events in any one
slice passed through the layers above it, the resulting Vp to Vs ratios were an
average of all ratios down to that respective slice. Thus, the ratio for each
individual depth slice was calculated by eliminating the averaging effect due to
any overlaying layers. The arrival times used for these calculations were from
the
events
considered
to
be
well
located.
Whether
a layer
boundary
representing the Moho was assumed to be at 60 km, 80 km, or any other depth
in that neighbourhood was immaterial, since the calculated Vp to Vs values
were 1.74+0.01 for all layers down to about 100 km. At this depth a large
increase
in the ratio was noted, to
- 27-
1.84±0.01.
Even after
taking into
consideration an increase in the P wave velocity, a pronounced S wave LVZ was
required to fit the results. Trying different upper and lower boundaries in the
calculations seemed to put this layer between 100±10 km and 130±10 km.
Despite not having a large number of events located below 130 km depth, all
layers below this point had Vp to Vs ratios of about 1.72±0.02.
The next step was to determine the parameters of the model, which were
governed by two factors. First, the total number of blocks was limited by
computational storage requirements, so that a large number of small blocks
was ruled out. Besides, blocks with small dimensions (less than 20 km to a side)
are poorly resolved in the inversion process. The second factor had to do with
the number of ray paths through each block, also an indication of how well a
block will be resolved. 20 rays through each block was set as the necessary
minimum of samplings needed to "see" it. On the other hand, it would have
been rather useless to use a small number of large blocks, each of which would
be sampled a very large number of times (e.g., a thousand or more times), thus
providing only redundant information. This was especially true for the region
in the center of the structure, an area with a high concentration
of
earthquakes. To determine the number of ray path segments passing through
each block, part of the three-dimensional velocity inversion program was used.
This was repeated using different block arrangements, until a satisfactory
balance in the number of samplings per block and their dimensions was
obtained. The locations of the events from the first relocation run were used as
the initial solutions for the partial velocity inversion runs. This procedure is
valid since stable solutions do not vary significantly from one model to another.
The block structure was extended to a greater depth in this run, so that the
upper mantle, including the S wave LVZ, could be adequately modeled. In this
manner, a larger number of intermediate depth events could be better located.
- 28 -
The resulting model is depicted in Figure 14.
Using the same selection criteria that were used for the first relocation
run, 442 events were considered to be well located. Nearly a hundred additional
events were
considered to have good stable solutions under the relaxed
criteria. This set of relocations showed the same trends as the previous set
when compared to the locations by Grange. However, the changes were smaller
in magnitude: on the average, the differences in latitude and longitude were of
about 5 km, approximately 7 km for the depths, and the new relocations
indicated that the origin times were about 0.5 to 1.0 sec later. Also, the RMS
values were about 0.1 sec less on the average. Once again, the errors in the
hypocentral
locations were about the same as Grange's.
In this set of
relocations, 92 percent of the reliable locations were among the events chosen
by Grange.
IV.
Final Observations
As a final comment on the relocations of these microearthquakes, it should
be
pointed
out that
the simple models used by
Grange were
a valid
approximation of a three-dimensional structure. The results he attained were
often very near the hypocenters calculated for the relocations, usually close
enough so that the uncertainty margins of both solutions overlapped. Also, it
should be noted that the few additional locations picked despite their larger
RMS, are valid solutions. The RMS residual is an indication of the effect of noise
within the data on the solution, and of the bias due to the model being used.
Since the RMS in all the flat layered and three-dimensional locations were about
the same size for most of the well located events, the bias due to the models
- 29-
could be considered to be small. Since we then knew that the noise in the data
was the major source of the RMS residual, we could relax the criterion
established by Grange for this parameter, provided that these solutions
converged and were stable for all models.
As could then be expected, the same seismicity patterns observed by
Grange (1983), described here in chapter 2, were noted. Despite having a
smaller set of earthquakes, the contortion zone of the Nazca plate could be
easily identified in cross-sections parallel to the Peruvian coast (Figure 15), and
in others parallel to the direction of motion of the Nazca plate (Figure 16). The
location of the bend clearly matched the northern end of the volcanic arc in
southern Peru. All three shallow seismicity belts were seen. The belts beneath
the coast and beneath the Western Cordillera were the most prominent due to a
greater number of events in these areas.
- 30-
CHAPTER 5
THREE-DIMENSIONAL VELOCITY INVERSIONS
The work done by Grange (1983) and by this author, show that the velocity
models used to relocate the earthquakes are reasonable approximations of the
crust and upper mantle under southern Peru. Nevertheless, these models were
somewhat limited.
Grange's locations and subsequent tests provided only
velocity models varying with depth.
The relocations performed with more
complex block structures were essentially only two-dimensionally varying
models. That is, the wave velocities changed only with depth and across the
profile made
perpendicularly
to the Peruvian coast.
Thus we felt that
performing a three-dimensional velocity inversion was the best method with
which we could gain some
insight into the complexities
due to lateral
heterogeneities of the Earth's crust.
I.
Procedure and Estimated Confidence Indicators
The inversions performed here used for starting models, the same block
structures
and
velocities
used
for
relocating
the
microearthquakes.
Simultaneously solving for the velocity structure and hypocentral solutions,
these calculations proceeded in an iterative fashion by making the changes in
the block's fractional slowness which best fit the residuals (see Chapter 3 and
Roecker (1982) for details).
- 31 -
The arrivals used in these inversions were from the 442 events cousidered
to be well located, and from 61 events with higher RMS. Besides having sta:le
solutions these additional events were chosen because they had a large number
of arrival times recorded, and most were located at depths greater than 70 km.
Before proceeding with the inversions, however, the first group of 442 events
was screened for events with less than 10 recorded phase arrivals located
within regions of high seismic activity. These events, while occupying the same
number of elements of the G matrix as events with a greater number of arrivals,
only provide small amounts of redundant information. When this selection
process was finished, 396 events were kept for the inversions. A list of these
events is found in Appendix A and plotted in Figure 17.
Three velocity inversions were carried out. The first used the same model
previously used in the second earthquake relocation.
The second inversion
used a slightly modified strucutre, in which the block interfaces parallel to the
coast were shifted inland in a northeast direction. This shift allowed a greater
number of blocks on the northeast side of the model with a sufficient number of
ray paths through them to be resolved. The final inversion was carried out
using a model in which the boundaries between the layers of blocks were
changed so that the Moho could be determined with greater accuracy.
A simplified map of the area was made as a template (Figure 18).
The
results for each layer of blocks were then overlayed on the map in four
different formats. First, the calculated P and the percent change from the
initial model velocities were shown superimposed on the map. Second, a map
was made which included the resolution and the standard deviation of the
calculated P velocity. The third and fourth formats were similar to the first two,
except that they used the calculated S velocities.
- 32-
Before proceeding with the analysis, some degree of
results had to be established.
nfiene
in the
A series of tests was performed by Roecker
(1982) to determine to what extent problems such as nonlinearity and improper
parameterization of the block structures affected the solutions to the inverse
problems. The data used in these tests were microearthquakes rec:rded in the
Pamir-Hindu Kush region of Central Asia. A summary of the criteria Roecker
established to interpret the inversion results follows:
(1)
The inferred velocities should be contourable. Trends should occur across
several blocks instead of being defined by the fluctuation of any one block.
This criterion is not only valid for variations within a layer, but from one
layer to another as well.
(2)
Large velocities at the edges of layers with few events are unreliable, and
extreme variations in regions of low seismic activity could be exaggerated.
(3)
A reasonable cut-off value for resolution is about 0.6 for P velocities. For
the S velocities, the cut-off is about 0.5 since the S arrivals are assigned a
smaller weighting.
(4)
For the array and types of anomalies studied by Roecker, variations in the
velocities smaller than 2% were probably insignificant.
Since the dimensions of the array and the magnitude of the anomalies
being studied in southern Peru were roughly the same as those in the ParnirHindu Kush region, the same lower limit on velocity variations was adopted.
Roecker estimated that the velocity variations for a given layer were
mainly due to the data from the events in that layer. Morever, one can usually
be confident that the large
scale variations of the calculated velocities
- 33-
oweer,
reasonably describe the actual!structure. It should be kept in maim ,
that any structural features presented by the initial model will
present in the inversion results.
sully be
The amount of change in the velocities
between the initial and resulting models is a more appropriate indicator of
whether the initial assumptions of the structure were reasonable or not.
II.
Analysis of the Inversion Results
Overall, the results of the inversions were similar to one amother. Several
characteristics stand out: First, there was good correlation between the P and
S velocities in each inversion down to about 70 km. Second, a velocity gradient
trending southwest-northeast exists within the crustal layers.
Third, the
resolution deteriorated with depth due to the decrease in the number of events,
especially below 100 km. Fourth, the data variance was considerably reduced
(by approximately 60 %), with the resulting variance being about equal to the
assumed noise level in the data (0.1 s). Finally, no resovable change in velocity
could be associated with the contortion in the Nazca plate.
The Crust
The top layer of the crust showed scattered results and low resolution
because of the geometry of the station network (Figures 19,20,33,34,47,48). For
the layers between about 20 km and 70 km depth, a gradient for both P and S
velocities was seen, with isovelocity contours roughly parallel to the alignment
of the model and the coast. Compared to the initial model, the gradient in the
results was smaller towards the edges of the structure and larger in the center.
The velocities decreased towards the northeast, under the Altiplano, and
-34-
increased towards the southwest because of the effect ac
se a ceire vnd
thinner continental crusts. The largest change noticed in the PanmdSeix citis
occured under the Western Cordillera of the Andes. The P vlocitisrwete in the
range of 6.1 to 7.0 km/s to the northeast of the Cordillera, and were in the
range of 6.6 to 7.6 km/s to the southwest. The results for these layers are
shown in Figures 21-26, 35-40, and 49-52.
The Upper Mantle
Below about 70 km depth, the velocity gradient disappeared.
Instead,
there seemed to be a zone in which the P velocity increased with depth
interspersed
with regions
of higher velocities
(Vp>8.0 km/s) and lower
velocities (Vs<7.5 km/s) (Figures 27-32, 41-46, and 53-58). Poor resolution did
not permit any interpretations below 130 km depth. Nevertheless, the smaller
regions of anomalous P velocities only stood out down to about 100 km. Below
this point there did not appear to be any large changes in P velocities. But one
should remember that poor resolution and the large scale of the blocks at this
depth may not have allowed us to resolve any small scale features that may
exist.
Within the mantle, the P and S velocities are not well correlated. The S
velocities did not show any small scale velocity anomalies, but only gradual
lateral changes in velocity with a high in the middle of the layers. Vertically, a
low-velocity zone could be noted in the layer between 100 and 130 km depth.
However, the velocity changes were such that no LVZ of the magnitude
indicated by the Wadati plots was noted. Poor resolution of the calculated S
velocities at depths greater than 130 km again did not permit any further
interpretations.
- 35 -
The Mohorovicic Discontinuity
As mentioned above, the initial model for the third velocity inversion was
designed so that a larger velocity contrast across the Moho could be detected,
at a maximum depth under the Altiplano of either 80 or 80 km. In the previous
inversions, a significant velocity contrast associated with the Moho could be
seen at about 70 km depth under the Altiplano, and at shallower depths under
the coastal region (Figures 25-28 and 39-42). The P velocities were at most
about 7.0 km/s above this boundary, and about 7.6 km/s or more below.
The results of the third inversion did not reflect any changes at either 60
or 80 km under the Altiplano as markedly as the two previous inversions.
Instead, it showed gradual velocity changes across these boundaries (Figure
51-56). This appears to indicate that under the Altiplano, the Moho is at about
70 km depth, and that the result of the third inversion is a consequence of
averaging the velocities above and below this depth.
The Bend in the Nazca Plate
Because of the small size of the three-dimensional structures used, only a
portion of the bend was included in our model. Unfortunately, this portion was
located in the northern part of the structure, a region of poor resolution. For
this reason, a small low velocity anomaly that could possibly be associated with
the bend was only resolved to a reasonable degree between depths of about 70
and 100 km.
Since only a few blocks with lower velocities matched the
approximate location of the bend, no definite correlation could be made.
The last two criteria established by Roecker (1982), summarized earlier,
were used to make contour maps of the percent change in P and S velocities
- 36-
with the epicenters of the earthquakes for layers 3 through 6 (Figures 57-ED).
In addition, a few profiles parallel to the direction of motion of the Nazca plate
were made and contoured in the same fashion (Figures 61-64). These figures
highlight the velocity anomalies within the crust and upper mantle beneath
southern Peru.
- 37 -
CHAPTER 6
SUMMARY AND CONCLUSIONS
The arrival time data set acquired in southern Peru during the summer of
1981 was used by Grange (1983) to locate a number of microearthquakes. This
author, using the same data, relocated these events using three-dimensional
structures to model lateral heterogeneities of the crust and upper mantle. The
results of these relocations were very similar to the original hypocentral
solutions
computed
by Grange,
indicating
that the
simple
flat layered
structures which he used were reasonable approximations to the actual
structure.
The tectonic characteristics of southern Peru were equally well
defined with either set of earthquake locations. The most prominent feature,
the bend in the Nazca plate as it is subducted under southern Peru, was located
beneath the northern end of the volcanic arc in the region. North of the bend,
the slab is being subducted at a shallow angle (10-15'), while south of the
bend, the slab is descending at a steeper angle (25 -300).
These observations
corroborated the theory of Barazangi and Isacks (1976;1979) that a wedge of
aesthenosphere is required between the overridding and subducted plates, for
subduction-related volcanism to occur. It was also shown that'the contorted
zone of the Nazca plate is parallel to the plate's direction of motion with
respect to the South American plate.
A subset of the well located events was then used to perform threedimensional velocity inversions in an attempt to model the seismic structure of
the region. Criteria established by Roecker (1982) to aid in the interpretation of
the inversion results were used. The features that appear from these results
- 38-
are the following: First, a velocity gradient seems to exist perpendicular to the
coast. The velocities are higher in the southwest crossing the Moho under the
coast, and decrease under the Western Cordillera of the Andes and the
Altiplano. Second, the Moho at its deepest point under the Altiplano, seems to
be at a depth of about 70 km. Third, the upper mantle seems to be a region
where P and S velocities are gradually increasing with depth, with the exception
of a few P velocity anomalies between 70 and maybe as much as 130 km depth.
The average velocities for this region seem to be in the range of 7.5 to 8.0 km/s
for the P, and 3.9 to 4.6 km/s for the S. The velocities for the anomalies were
greater than 8.0 km/s and less than 7.5 km/s. Finally, an S wave low-velocity
zone ts seen between 100 and 130 km depth. However, it does not seem to be as
pronounced as it was originally thought to be, when Wadati plots were made to
determine Vp to Vs ratios for different depth slices.
_W , MAWN LP
SIXx 57RAWT PAK
.w rc avrgm
acIE
Xr a/ 6W a qSw /rr
Trudeau (1975)
- 39 -
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Pavlis, G.L., and J.R. Booker, The mixed discrete-continuous inverse problem:
Application to the simultaneous determination of earthquake hypocenters
and velocity structure, J Geophys. Res., 85, 4801-4810, 1980.
Plafker, G., Alaskan earthquake of 1964 and Chilean earthquke
implication for arc tectonics, J. Geophys. Res., 77, 901-925, 1972.
of
1960:
Roecker, S.W., Velocity Structure of the Pamir-Hindu Kush region: possible
evidence of subducted crust, J. Geophys., Res., 87, 945-959, 1982.
Rutland, R.W.R., Andean orogeny and ocean floor spreading, Nature, 233, 252255, 1971.
41 -
Spencer, C., and D. Gubbins, Travel time inversion for simultaneous earthquake
location and velocity structure determination in laterally varying media,
Geophys. J R. astr. Soc., 63, 95-116, 1980.
Suarez, G., Seismicity, tectonics, and surface wave propagation in the Central
Andes, Ph.D. Thesis, M.I.T., 260 pp., 1982.
Suarez, G., P. Molnar, and B.C Burchfiel, Seismicity, fault plane solutions, depth
of faulting, and active tectonics of the Central Andes, J. Geophys. Res., 88,
10,403-10,428, 1983.
Suarez, G., J Gagnepain, A Cisternas, D. Hatzfeld, P. Molnar, L. Ocola, S.W
Roecker, and J P. Viode, Tectonic deformation of the Andes and the
configuration of the subducted slab in central Peru: results from a rmcroseisrmc experiment, submitted to Geophys. J. R. astr. Soc., 1984.
Swift, S.A., and M.J. Carr, The segmented nature of the Chilean seismic zone,
Phys Earth & Planet. Int., 9, 183-191, 1974.
Thurber, C.H., Earthquake locations and three-dimensional crustal structure in
the Coyote Lake area, central California, J Geophys. Res., 88, 8226-8236,
1983.
Trudeau, G.B., Wouldn't a Gremlin Have Been More Sensible?, Bantam Books, New
York, 1975.
- 42-
FIGURE CAPTIONS
Figure 1. Earthquake locations used by Barazangi and Isacks to infer a tear in
the Nazca plate as it is subducted under southern Peru. From Isacks
and Barazangi (1976), and Barazangi and Isacks (1979).
Figure 2. a) Vertical cross sections of earthquakes relocated by Hasegawa and
Sacks inside rectangles shown in the inserted map. Solid line is the
assumed shape of the seismic zone inferred from the seismicity below
a depth of 50 km.
b) Map of local seismic network used by Hasegawa and Sacks.
c)
Subduction model
proposed
by
Hasegawa
and Sacks. From
Hasegawa and Sacks (1981).
Figure 3. Vertical cross sections of earthquakes perpendicular to the trench,
and their locations on a map. All earthquakes were located by Grange
(1983) and are considered to be reliable. Fault plane solutions are
back hemisphere projections
with dark compressional
and light
extensional quadrants. "T" indicates the position of the trench, "C"
the position of the coast. Triangles at the top of some sections
indicate the position of active (open triangles) and dormant (closed
triangles) volcanoes. In some sections the Mohorovitic discontinuity,
as inferred from the model of Couch et al., (1981), appears as a dotted
line. From Grange (1963).
Figure 4. Vertical cross sections of earthquakes parallel to the trench, and
their locations on a map. Symbols are the same as in figure 3. From
Grange (1983).
-43-
Figure 5. Maps of reliably located earthquakes at different depth intervals.
From Grange (1983).
Figure 6. Vertical cross sections of earthquakes parallel to the direction of
underthrusting of the Nazca plate, and their locations on a map. From
Grange (1983).
Figure 7. Map of all epicenters with contours for events in different depth
ranges. Note the change in orientation of contours from being parallel
to the coast to more northerly trends near 150 to 15.50 S. Open
triangles show locations of active volcanoes, closed triangles dormant
ones. The arrow to the left gives the direction of relative plate motion
between the Nazca and South American plates. From Grange et al.,
(1984b).
Figure 8. Maps of reliably located earthquakes at different depth intervals with
fault plane solutions. Fault plane solutions are lower hemisphere
projections with dark compressional quadrants and light dilatational
quadrants. From Grange (1983).
Figure 9. Map with locations of seismic stations in southern Peru. Latitude,
longitude and depth for each station is listed.
Figure 10. Configuration of three-layered structures used by Grange (1983).
The sections labelled 1, 2, and 3 show the limits of the three simplified
structures used to approximate the thickening of the crust. Note that
these limits depend on the relative postition of the event and the
station.
Figure 11. Profile of first model used to relocate microearthquakes. Numbers
are P and S velocities of different parts of the model.
-44-
Figure 12. a) Structure proposed by James (1971) for Bolivia and southern Peru.
b) Depth contours for the Moho proposed by James (1971).
Figure 13. Wadati plots for different depth intervals. Plotted points are P minus
S arrival times vs. P arrival times.
Figure 14. Profile of second model used to relocate microearthquakes.
Also
used as the initial model for velocity inversions. Numbers are P and S
velocities.
Figure 15. Vertical cross sections of relocated earthquakes, parallel to the
trench,
and their locations
on a map. These
earthquakes
are
considered to be reliably located.
Figure 16. Vertical cross sections of relocated earthquakes parallel to the
direction of underthrusting of the Nazca plate, and their locations on
a map.
Figure 17. a) Map of all relocated earthquakes used in the velocity inversions.
b) Maps of relocated earthquakes at different depth intervals with an
outline of the three-dimensional
structure
used in the velocity
inversions.
Figure 18. Simplified map used as a template to display the the calculated
three-dimensional velocity structures.
Figures 19 - 58. Maps displaying calculated values for P and S velocity
structure. On each page, the top map shows the calculate velocity and
the percent change from the initial model for each block in the
specified layer, and the bottom map shows the resolution and the
standard deviation of the calculated velocity for each block. At the
-45-
bottom of each page the number of the inversion run, the upper and
lower bounds of the layer, and the type of phase used (P or S) are
specified.
Figures 59 - 61. Contour maps of the percent changes in P and S wave velocities
for the first inversion. The configuration of the blocks used in the
inversion is superimposed upon the seismicity maps.
-48-
a .W.
Po
t
T
cLCa
unLM
OF SMOUrRN ptjU
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00
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-48 -
*
4
00
j
0
oo
S
DISTANCC (KM)
m
0
0
.
50*
0SO
5u.
o.
-47-
18 S
19 S
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Figure 3.
-48-
I7.
0
T
A13
Figure 3(cont.).
-49-
200A
300
O00
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is
s
u
is s s
NW
oo
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thu
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v
soo
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2000
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84
Figure 4.
- 50 -
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0
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812
oo
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200
200
190
200
89
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813
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o.
200
81t
Figure 4(cont.).
- 51 -
0
120-1 4 0 km
S"
-
I
1
*.
as
Figure 5.
- 52 -
.
i
It
S
Is S
I.
S
17 S
is
T100
S
200
300
01
T
C
c2
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A
AAAAAAA
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200
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100
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Ca
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Figure 6.
-53-
*
.0,
14 S
15 5
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.
S ', \
1- S
I-.
.
,
-- -
S
19 S
76 W
75 w
74 W
73 W
Figure 7.
- 54-
IS S
17 S
is S
Figure 8.
- 55-
ld
I
Station
Latitude S
Longitude W
YAN
CAL
CHO
PAT
CAB
LLU
CRV
ARE
AYE
ONG
TOR
SIS
CAY
MOL
RA r
15' 32.09'
03. 74'
08.00'
71' 21.03'
71' 22.21'
71* 47. 71'
45. 47'
710
39. 62'
10. 65'
47. 07'
27.73'
00.80'
53. 94'
20. 46'
18. 13'
21.25'
00.52'
45.33'
29.89'
29.62'
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71*
72*
73*
710
710
72'
720
72'
710
72'
720
72"
71t
72'
SIQ
CAN
SGP
16'
15*
15*
15*
16'
150
16'
17'
15'
16"
16'
16'
170
15•
15
16'
160
Figure 9.
- 56-
39.44'
56.66'
02. 11'
28.38'
29.48'
40.31'
28.39'
28.25'
04.85'
66. 45'
02.88'
43.62'
45.06'
55.79'
42.75'
Altitude
4050
3950
4500
4900
3770
1800
1780
2452
240
880
350
1475
1700
50
4000
4550
1200
140
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er
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Figure 12.
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440
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p
Top o f If
o
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93to.l
k.
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Up / UV * 1.72.o
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Figure 13.
- 60-
ttgw
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km.
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(Wi')
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Figure 15.
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Figure
15(cont.).
- 63 -
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Figure 16.
- 85 -
Depth ranges
* - 300 km
Sela te (50 km)s -
ALL SLUATS
14
17
18
Figure 15(cont.).
-84-
O.
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Figure 1.(cont.).
18(cont.).
- 66-
.
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Figure 16(cont.).
- 687 -
ALL av4mT
Depth raft"
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epth r age
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Figure 17.
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(0
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km
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to
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tate (3 km)I -
Figure 17(cont.).
-
89 -
Depth
rw'p In
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gusto ( m )3 -
Figure 17(cont.).
-
70-
-
13 b
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(SO km)~
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Figure 18.
S
S
I
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C
Si
I'
- 71 -
16
S*
S
Figure 19. 1; -5 to 5 km; P
- 72 -
11
11 73
71
73
14
I5
0.49
0.08
0.3
15
18
to
0..1
0.61
0.SS *.oo
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0.04
0.67
74
70
0.80
0.03
17
0.68
0.80
0
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Figure 20. 1; -5 to 5 km; S
- 73-
3
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14
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w
ti
.
t.
6,37
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3
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73
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738
7
14
I
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6.18 6.04
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1.
5.96
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5.76
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S.66
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15.
i
11
s15
71
7
70
16
70
0.13
0.74
0.57
0.608
**9
17
.
O.0
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0.57
0.91
0.13 S.
0*84 S."
00
0.11
0.St
0*16
0.73
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1
Ar
7W
1W
*-
r-
Figure 21. 1; 5 to 20 km; P
- 74 -
7
,
7,
17
is
1
18
Figure 22. 1; 5 to 20 km; S
- 75-
79
17
1i
70
17
1
Figure 23. 1; 20 to 40 km; P
- 76-
74T.
4a37
4,08
4.04 .,
4.1 4.j
4.48
3.
4.464 4.0
9.
-i.
4.
3
81
3
3.
to
73
71
78
14
is
70
16
7.
::
74
:
:
17
$::
20 to 40 km S
Figure 24. 1; 20 to 40 km; S
-77-
"
79
IS
7,
17
1
Figure 25. 1; 40 to 70 km; P
-78-
7.
17
1
16
Figure 26. 1; 40 to 70 km; S
- 79 -
I
'lq
70
i
A
7t
is
1
7.46
?
1r
i
7494.
7
7
-.
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7.
soot
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8,
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7.3
7.0
17
8.
71r9
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7.
7s
1
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-r
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1
Figure 27. 1; 70 to 100 km; P
- 80 -
\r
14
3
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a
.
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.
71
15
..
..
::
1
7.
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17
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its
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Figure 28. 1; 70 to 100 km; S
- 81 -
77.
13
11
14
3
0.13
-M
74
7a
71
70
*o?
0*.4
17
is
-j
Figure 29. 1; 100 to 130 km; F
- 82 -
55
7f
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71
14i
4*.47
4*r.
4r
4.
41
is
IS
74
73
14
17
7
71
7
715
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i
7@
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13
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to
:0
Figure 30. 1; 100 to 130 km; S
- 83 -
*
'
a
14
71
71
15
70
17
74
1
Is
74
73
14
17
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78
71
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71
7
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0.14
1
70
1.
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17
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Figure 31. 1; 130
Figure 31. 1; 130 to 160 km; P
-84-
7
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78
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AS
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73
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3
7
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Figure 32. 1; 130 to 160 km; S
- 85-
70
17
18
Is
17
18
Figure 33. 2; -5 to 5 km; P
- 86 -
17
is
70
17
Figure 34. 2; -5 to 5 km; S
- 87 -
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Figure 35. 2; 5 to 20 km; P
- 88 -
70
1?
Figure 36. 2; 5 to 20 km; S
- 80-
70
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17
18
Figure 37. 2; 20 to 40 km; P
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7.
17
18
18
79
17
18
Figure 38. 2; 20 to 40 km; S
- 91 -
70
17
70
17
Figure 39. 2; 40 to 70 km; P
-92-
70
1?
13
16
Figure 40. 2; 40 to 70 km; S
- 93 -
70
18
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70
17
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Figure 41. 2; 70 to 100 krn; P
-94-
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73
71
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4.39
16
4.37
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4.48
a.
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0.?13
0.14
0.68
0.14
7e
17
0.33
0..15
74
Is
13
1f
rJ
ra
Figure 43. 2; 100 to 130 km, P
- 96 -
1.5
a
'1
r&
N
14
73
71t
1
4.
10
4.43
3.
4.74
10.
4.49
4.
4.1
4.35
4.
4.43
-I.
17
14
73
0.15
.
.
6.
17
3.
73
78
71
78
1is
7'
70
0.36
0.10
0.80
0.07
0.78
0.6
7,
0.a4
S.o
0*75
17
0.0781
e.07
0.0?
...............................................
18
£-r
Irf
re
Figure 44. 2; 100 to 130 km; S
- 97 -
&*
*11
7g
r4
TS
71
78
1
16
7.76
-3.
7.89
-4.
7e
17
3.14
3.
18
17
1n
73
71
7,
17
18
Figure 45. 2: 130 to 160 km; P
- 98-
"r
N
14 17
78
71
4.84
5.
tS
4.
7.
18
4.59
17
-0,
1i
714
73
17
73
71
72
14
71
7I
Is
70
1
16
0.44
0.10
0.08
7.
8.57
17
8
i
&
Figure 46 2; 130 to 160 km; S
- 99 -
7
r
18
73
14
78
71
is
70
1.17
5.01
-4.
5,7
5.99
-2.
5.744.68
10. -11.
1.
5.09
-8.
5. 0
-4.
S.74
8.
6.106.38
17. 12.
5.47 5.114.7
3. -4.-19.
5.33
-1.
S.11
-5,
5.13
-1.
4.87
-6.
5.89
13.
70
17
5.44
i.
18
4
73
14
17
73
d
71
7a
14
15
in .
1
7"
0.83
O.88
0.86
0.48
0.43 0.89
0.10 90.88
0.61
0.07
0.760.48
0."80.98
0.17
0.06
0.42
0.08
70
9. a
0.07
0.810.77
9.100.18
0.83 0.800.68
.10 0.070.ee
0.49
0.13
O.S5
S.31
e.
" 3; -5 to
Ol"5 km; P18
gure7.
Figure 47. 3, -5 to 5 krm P
- 100 -
17
is
314
v
-
ii
--
$i-
~
3.
.
3.10
3.01
3
3.393.00
13. -0.
3.
3.34
g.
74
3.04
.
3.34
3.7
73
3.17
3.33
?. *0.
.73.
71
14
0..
0.4
1."
8
0 .830.1
0.780.51
74
0.04
9g
1
0.31 0.8
0
.
13
t
17
c
07
.40.5
O.O
70
0..4
0.06
O.
71
7
7
17
-*74
.a
-7.
a.
-41.
.
17
3.8 3.,4
It*
, II!
O.8
0.36
O31
O.Ol
Figure 48. 3, -5 to 5 km, S
- 101 -
70
17
18
\
71
"UB
i1
I-
A"
is
1'
e,
0.10
:
: 8:
tl
OR
0"0.
4 II
6.19
17
0,
: :8
0*94
~.~~
~88
:U U:.
- -m
13
-mN
ITP
Figure 49. 3; 5 to 30 km, P
- 102 -
1,,
7!
L
t
70
17
71
732I
15
i
7.
0."
17
S
7
;3:M
:8
014 t: G
,: *::5
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$:
eI:s
ona
.M8.3
0,?
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0.
,94
'*
*: .09*4
:
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17
I
T-
Figure 50. 3; 5 to 30 km; S
- 103-
-r
--I
se
r
gain
is
71
T7
S1o
.
.
-4*
73
-as
Is
4.
13
1s
'71
73
14
7.
71
817
7
7.4
to
3.
-*
4.
3.
3.
3.
\
17
0.
s
S
L.
1
Ao
71
7
1
1
0.11
CO7
0.4
6.13
**0
0,0*7
0.13
7,
0.1
17
6..1
..,1
:8
O.
0.10
09.
0.*4
0. 14
:
19
-I
-w
gure
5.
3
30
60
k;
P
Figure 5,. 3; 30 to 60 km; P
- 104-
1,I
i
4.41
74
1.
4.
4.38
.
3.
-3.
fj
4..4
3
r
3.M
17
131
73
14
71
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7.
15
is
73
I
07
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C•:
e.900:.9
:: r
,:: 0.04
::0.07 03~.
0.
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0.
5 3 30 o 60 k
Fre
17
Fiaure 52 3; 30 to 60 km; S
- 105-
'.***9
7.
7.t
t1.
73
•.
7o3M
174
7.
- 1q
7
-.
.1$
7.8
7
741
.
to4
1.
7.1
- .
7.16
g.
773
4
7
so.
6
-,.
1
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70
* 14
e.54
0.63
:.a
0: s
.
0.14
0.1
1
7
W
0.36
0.57
.11
0.13.
F74 re 53 3; 60 to 0 k,
P11
Ftgure 53 3; 60 to 80 km, P
- 106-
Figure 54. 3; 60 to 80 krn; S
- 107 -
14
?.
73
." 7
7.61
-1.
7.7
7. a.
7.3
7..
7
7.8
4.
1
7,7
7
7.98
6
4.
7 .-
7.43
7.35b
-4.
17
18
I r
F%7
I*
7I
7.
17
13
Figure 55. 3; 80 to 100 kin; P
- 108-
*
71,
7-3
'*
4.46
4.41
.
4
4.
4.47
4.
4
4.4
46
4
4.
.
1.
9.
1.
-4.
1is
-1.
.
4.4
7
is
18
74
:
,a
0,s
17
78
3
0.45 0.73 0.73
0.97 0.07
*.O
:e '.38
8.
cis
son
Se.eU
"
'n
0.53
0.09
0.1
.*
o
O
11
30.1
17
Figure 56. 3; 80 to 100 km; S
- 109 -
L
qm
I
ve
It
6.
-4.
7.75
3
7.71
-.
3.18
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-a.
7,.5
-3.
is
16
8.1
3.
8.16
3.
8.
7.
17
8.
i3
j7
4gW
1ram
ri
-i
16
Is
79
17
18
Figure 57. 3; 100 to 130 km; P
- 110-
rr
L
77
ri
i
494
1l
4.7
4
4
70
1I
4,4
4..
441
4.43
5.
3.
-3.
3-
433
1.
17
Is
I
I
17
' 4
73'
14
11
r
rJ
71
73
is
71
7.
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16
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0.7
e.08
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e~~I.?
70
*
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38
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r
Figure 58. 3; 100 to 130 kmn; S
-
111 -
a
DY
4
isN
42
Y.
*
I
14
cr)
75
171
Layer
Layer 6
4,
70T -100
km
70 - 100 km
2
04
0I
8 phase
P phase
APPENDIX A
This appendix contains a list of the 396 events used in the velocity
inversion. These locations were determined in the second relocation run and
are considered reliable.
The following information is presented for each
earthquake:
(1) Number used as a reference during this study.
(2) Date (year, month, day).
(3)
Origin time (hour, minute, second).
(4) Latitude, longitude, and depth.
(5)
Magnitude determined by Grange (1983) using the duration of the coda T in
seconds and the formula ML = -1.1 + 2log[H + 0.007Z + 0.0035D where D is
the epicentral distance and Z the depth at which the earthquake occurred
(modified from Lee et al., 1972).
(6) RMS - root mean square of the time residual.
(7) GAP - maximum azimuthal aperture without stations measured from the
epicenter.
(8) DMIN - distance to the nearest station.
(9)
Number of recorded phases.
- 115-
number _date__
7
9
10
11
12
19
32
37
41
46
48
50
54
58
59
68
74
75
76
77
87
88
89
90
91
94
101
105
112
118
125
129
132
148
160
167
171
172
175
176
199
201
203
207
209
210
23
1
2 :
3
3 :
7
15 :
17 :
23 :
2
3
4 :
7
7 :
7 :
15
0:
0 :
0 :
5
6
6
7
7
8
11
13
18
22
5
7
9
2
27.7
4.1
33.3
48.6
28.4
37.3
33.0
43.7
57.4
39.8
52.7
52.0
49.8
35.7
33.7
29.5
13.2
37.1
6.0
31.1
10.0
:
:
:
:
:
:
:
:
10 :
81
6
12
latitude
time
19
21
22
5
5
19
20
21
0
0
1
:
:
:
:
:
8
45.4
13.4
40.3
48.5
47.6
40.7
31.1
27.6
32.1
43.9
42.1
50.4
54.7
45.8
16.0
41.3
39.5
27.9
45.8
5.9
52.4
16.6
18.6
12.6
: 9.9
16.14
16.90
15.15
16.24
16.30
16.21
15.54
16.27
16.12
16.67
16.73
16.15
15.88
15.33
16.30
16.54
15.05
14.69
16.49
15.98
16.80
16.78
16.15
16.56
16.78
16.30
16.65
15.83
16.85
15.03
15.62
15.31
16.66
15.24
16.59
16.50
16.36
15.06
17.96
16.93
16.04
16.72
16.34
16.05
15.58
16.66
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
longitude
72.00
72.83
72.28
72.17
71.62
72.38
73.80
73.04
72.46
72.56
72.61
72.52
72.50
71.73
71.96
71.47
71.99
72.37
72.28
73.36
71.51
72.26
73.03
72.45
72.73
72.11
71.88
71.55
72.77
72.39
72.77
72.85
71.92
72.37
71.69
71.80
72.28
71.86
72.63
72.89
71.74
71.74
71.97
72.32
71.41
72.40
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
depth
(km)
magnitude
RMS
GAP
(deg)
DMIN
(km)
107.6
17.6
98.0
24.3
123.4
104.4
90.5
65.6
100.2
57.4
56.0
24.9
105.9
124.6
96.7
38.8
118.5
95.6
80.0
76.7
38.6
28.5
84.0
40.7
32.4
15.6
30.9
141.2
51.7
104.6
107.7
197.4
83.6
107.1
95.0
93.4
82.3
121.1
8.7
20.2
124.6
26.7
18.0
117.0
145.1
33.2
3.3
3.0
0.229
0.079
0.014
9.134
9.073
0.107
0.911
0.278
0.321
0.044
0.180
0.011
0.250
0.178
0.219
0.009
0.153
0.164
0.239
0.172
0.239
0.012
0.228
0.014
0.222
0.136
0.244
0.057
0.108
0.008
0.033
0.236
0.279
0.152
0.079
0.051
0.210
0.162
0.048
0.020
0.194
0.180
0.147
0.151
0.115
0.146
92
268
263
130
253
118
313
247
80
254
201
168
183
135
133
287
230
284
144
217
255
286
200
269
215
166
140
110
224
238
209
208
235
196
259
240
153
250
301
271
140
131
177
167
147
284
5.5
38.8
63.2
15.3
17.9
36.8
43.9
47.8
24.2
20.4
21.9
21.4
28.4
22.9
12.5
39.0
23.3
79.5
25.7
24.9
56.6
53.4
54.1
24.4
56.1
3.0
34.7
14.4
64.8
55.1
13.2
23.8
36.8
62.4
52.6
37.2
20.7
10.6
55.1
44.3
34.5
33.5
12.5
33.5
8.0
36.3
2.3
3.5
3.3
3.4
4.8
3.9
2.6
2.6
1.7
3.1
3.9
2.8
4.0
2.9
3.4
2.6
2.7
3.2
2.8
3.2
2.1
4.4
4.1
3.5
4.6
3.8
3.9
2.7
0.
2.4
2.5
3.2
2.8
3.2
4.1
number
phases
number
229
224
229
231
232
233
241
253
255
256
260
263
265
268
269
270
272
275
279
291
295
305
306
309
310
311
316
317
322
323
328
332
333
336
340
342
343
353
355
359
362
363
364
367
369
372
date
time
latitude
4.0
40.4
9.8
6.2
53.1
33.0
21.4
13.0
36.8
14.2
2.0
7.2
40.6
57.2
20.7
15.1
45.9
36.5
5.9
43.5
57.5
61.1
9.6
36.0
34.5
9.7
15.6
10.3
8.4
17.5
43.7
8.1
43.3
13.2
11.3
55.0
18.1
17.7
61.3
3.7
40.2
21.1
6.7
50.9
26.7
33.3
15.93
16.27
16.72
16.63
16.70
15.15
15.98
15.83
15.87
16.43
16.20
16.56
15.76
17.20
16.65
15.08
16.19
15.44
16.03
16.44
16.35
16.27
15.84
17.31
15.13
16.25
16.08
14.93
16.00
16.42
16.92
17.05
16.20
15.03
16.18
16.78
16.32
16.98
15.86
16.04
16.01
16.36
14.89
16.21
16.09
16.78
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
longitude
depth
(km)
magnitude
RMS
GAP
(deg)
DMIN
(km)
72.90 W
72.23 W
72.58 W
72.65 W
72.68 W
72.04 W
73.52 W
73.39 W
71.50 W
72.05 W
72.04 W
72.72 W
73.68 W
71.83 W
72.66 W
73.72 W
73.27 W
73.61 W
73.15 W
72.87 W
72.06 W
72.48 W
73.78 W
71.46 W
72.35 W
73.98 W
72.38 W
72.46 W
72.26 W
71.909
71.18 W
72.22 W
71.81 W
72.22 W
71.73 W
72.29 W
72.55 W
72.90 W
72.62 W
72.94 W
72.46 W
72.58 W
71.99 W
72.08 W
72.43 W
72.19 W
101.1
99.6
60.8
57.3
50.8
123.2
69.2
82.9
142.8
23.2
17.8
37.9
82.9
52.2
58.6
125.8
65.5
4.2
0.181
0.300
0.036
0.114
0.105
0.377
0.072
0.205
0.257
0.199
0.169
0.196
0.066
0.349
0.040
0.187
0.237
0.200
0.057
0.222
0.195
0.244
0.161
0.300
0.282
0.144
0.152
0.155
0.267
0.257
9.155
0.212
0.105
0.327
0.076
0.127
0.280
0.045
0.195
0.252
0.294
0.025
0.158
0.128
0.136
0.195
142
87
252
199
202
201
247
161
155
207
116
192
318
267
247
290
209
297
165
190
159
124
319
294
211
189
151
239
188
132
312
241
230
226
183
164
88
274
165
139
119
160
293
161
144
142
27.1
16.7
43.2
9.9
15.1
26.8
22.6
10.1
20.9
14.3
2.8
1.2
22.1
26.3
11.6
82.8
50.5
92.3
44.2
21.6
5.3
8.4
33.7
39.8
58.8
52.2
30.1
70.6
30.8
14.8
60.4
19.5
17.9
47.5
20.3
36.0
8.7
49.7
16.2
39.2
12.0
11.7
34.7
6.5
28.2
29.7
105.8
69.0
61.5
22.0
100.5
81.2
77.8
113.7
71.6
21.5
106.8
107.7
19.5
183.2
54.7
144.0
103.4
118.1
40.4
96.6
28.0
185.285.0
15.6
85.4
189.5
12.5
20.1
38.6
2.7
3.1
3.5
4.8
3.9
3.3
4.1
2.0
2.0
3.2
3.8
3.4
2.8
4.5
3.5
4.3
2.3
3.2
2.7
3.5
3.6
4.0
3.3
2.2
4.5
2.8
2.7
2.7
3.7
3.0
2.6
4.2
2.9
3.0
3.1
2.2
2.7
3.5
1.6
1.8
2. 8
number
phases
number
373
374
375
376
379
380
381
382
383
384
387
388
389
391
394
401
402
404
406
407
409
412
416
417
418
4290
422
424
428
431
433
436
437
441
443
444
447
450
451
453
455
462
468
471
474
477
_date_
time
latitude
28.8
16.6
55.1
59.3
44.4
32.8
52.5
32.1
14.3
18.1
56.9
23.7
9.4
27.8
32.2
38.0
7.8
52.2
60.0
9.8
15.4
53.7
59.8
35.5
22.5
31.1
10.2
25.4
8.3
49.0
48.7
23.1
9.9
19.5
43.6
11.7
56.9
41.6
1.2
13.2
56.5
56.3
39.7
42.8
16.1
54.6
16.27
16.17
15.97
15.61
16.02
16.32
15.76
16.80
16.81
16.24
16.19
17.32
17.11
16.12
16.42
16.15
16.01
16.14
16.37
16.28
16.81
16.75
16.42
16.25
16.72
16.22
15.70
15.74
16.76
16.89
16.11
15.95
15.17
16.53
16.92
15.89
16.99
16.16
16.35
16.04
16.32
15.79
15.80
15.92
16.67
15.81
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
longitude
72.27
72.38
73.24
71.91
72.36
71.85
73.30
71.46
71.80
72.83
72.39
72.57
71.54
72.41
72.68
71.65
72.48
72.21
74.02
72.69
73.16
72.56
72.64
72.00
73.18
72.54
73.75
72.42
72.57
72.89
72.90
73.80
72.45
73.57
72.11
72.64
72.92
72.64
72.24
72.90
72.56
72.94
72.54
73.37
71.86
72.56
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
depth
(km)
magnitude
RMS
GAP
(deg)
DMIN
(km)
104.8
97.1
92.0
13.1
22.4
18.6
85.1
77.7
81.6
16.8
84.9
8.4
69.2
185.2
66.8
19.8
100.9
27.7
57.3
87.8
37.6
58.3
84.4
16.7
47.3
25.6
90.0
110.1
53.3
40.8
45.7
75.6
189.2
57.7
12.2
101.1
42.7
31.5
90.1
91.4
82.8
102.5
105.8
84.7
46.0
105.4
3.4
2.6
3.1
1.9
2.3
2.1
2.8
2.9
3.0
1.9
2.6
3.6
2.8
3.2
3.4
2.6
2.7
2.1
4.0
4.2
2.9
3.2
3.2
2.1
2.8
2.3
3.6
3.6
3.5
2.8
0.167
0.175
0.319
0.213
0.151
0.066
0.180
0.053
0.148
0.118
71
135
170
251
160
141
186
258
142
122
114
260
298
139
116
210
115
153
303
118
272
200
223
148
272
132
307
137
202
235
142
302
288
274
152
91
244
157
80
186
89
130
122
189
136
119
28.4
25.7
31.9
8.7
17.6
8.6
18.2
32.6
26.4
7.1
33.3
65.7
17.6
25.2
16.5
26.2
12.9
19.6
87.5
24.5
54.8
26.9
19.9
9.2
52.6
15.6
31.0
18.7
26.7
41.2
43.5
39.7
70.4
82.7
12.1
17.1
52.2
26.9
17.6
36.9
9.5
23.3
12.7
18.8
36.5
13.5
3.8
3.6
2.7
3.2
3.3
3.3
3.4
2.7
3.6
4.1
3.0
3.0
3.5
0.070
0.136
0.017
0.102
0.264
0.148
0.066
0.090
0.328
0.476
0.189
0.153
0.094
0.144
0.082
0.092
0.241
0.218
0.244
0.312
0.407
0.157
0.283
0.072
0.070
0.293
0.120
0.193
0.190
0.104
0.248
0.085
0.198
0.189
0.154
0.181
number
phases
number
478
479
480
484
489
491
498
500
502
504
509
512
513
519
525
529
530
531
532
538
540
541
543
549
555
558
561
562
568
572
573
575
580
584
585
590
591
593
594
597
601
602
603
605
611
617
time
_date_
20
21
21
0
6
7
13
15
18
20
1
4
6
6
7
8
9
10
15
17
17
17
19
23
2
2
3
6
10
10
13
17
20
23
2
1
5
6
7
9
9
9
11
13
20
59
5
42
17
12
43
1
23
6
14
22
3
6
32
28
43
50
36
17
13
18
43
30
27
6
46
4
0
19
38
47
47
5
42
26
49
11
24
18
49
14
0
12
54
31
13.8
33.0
57.9
: 34.9
= 48.4
25.0
32.7
51.0
27.9
8.8
1.9
58.1
41.7
18.6
43.6
59.1
21.7
29.5
47.0
: 59.8
: 37.2
: 48.0
: 26.8
: 54.7
: 16.5
4.5
: 34.9
: 58.5
: 47.1
: 20.9
: 42.0
: 22.6
: 19.0
: 57.1
: 37.7
: 480.0
: 24.5
: 38.8
30.1
45.2
49.9
56.5
6.6
:16.0
16.4
36.1
latitude
16.24
14.59
16.48
16.83
15.72
16.69
15.76
16.22
16.19
16.22
16.31
15.78
16.43
16.32
15.99
16.43
16.77
16.28
17.49
16.34
16.59
15.83
16.14
16.63
16.34
15.89
16.07
15.12
16.26
16.02
16.29
15.35
16.08
15.58
14.89
17.14
15.79
15.88
15.93
16.07
16.19
15.96
16.63
15.23
15.51
15.60
.S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
longitude
depth
(km)
magnitude
RMS
GAP
(deg)
73.34 W
72.20 W
72.45 W
71.27 W
71.65 W
72.54 W
70.38 W
73.20 W
72.07 W
72.72 W
72.02".W
72.45 W
71.98 W
71.88 W
72.22 W
71.82 W
72.53 W
72.98 W
72.09 W
72.32 W
71.62 W
73.69 W
72.98 W
72.74 W
72.35 W
73.36 W
73.73 W
71.53 W
72.07 W
72.25 W
72.40 W
72.98 W
73.70 W
73.09 W
71.97 W
71.21 W
72.58 W
73.59 W
71.91 W
71.76 W
72.15 W
72.96 W
72.45 W
72.17 W
72.42 W
71.19 W
49.3
97.7
77.2
92.3
140.6
58.4
214.4
73.9
101.8
92.5
25.7
114.2
27.1
111.3
99.9
93.6
59.4
82.4
29.0
79.1
8.8
78.7
94.8
56.0
83.8
84.6
68.5
139.9
22.9
105.1
100.3
197.1
73.3
95.1
112.5
87.1
101.0
77.3
129.2
129.3
187.3
98.9
38.8
103.3
110.7
162.9
3.5
4.4
3.4
3.2
3.5
2.6
4.5
3.3
0.386
0.279
0.266
0.041
9.1108
0.043
0.369
0.130
0.055
3.2
2.4
4.6
2.3
3.2
3.1
2.9
2.9
0.442
228
277
89
290
124
242
290
201
128
122
147
90
188
150
217
135
200
238
287
147
115
309
244
237
126
176
283
251
121
205
102
211
279
189
258
283
81
280
76
164
155
131
216
208
162
252
3.2
2.8
3.3
3.4
4.4
2.9
2.9
3.6
4.7
3.0
3.2
4.1
3.6
4.6
3.7
3.8
3.5
3.1
3.3
3.4
2.9
3.9
2.2
3.7
4.2
0.141
0.180
0.043
0.315
0.109
0.097
0.106
0.304
0.378
0.145
0.291
0.181
0.179
0.376
8.427
0.028
0.204
0.269
0.210
9.129
0.272
0.117
0.257
0.201
0.272
0.449
0.212
0.178
H.123
0.084
0.139
0.226
0.153
8.229
0.306
0.151
DMIN
(km)
52.6
82.5
6.9
48.0
4.1
22.9
107.1
56.2
4.2
38.5
7.0
13.5
23.8
12.1
28.6
10.3
29.9
43.0
53.8
16.9
14.0
24.2
50.3
7.8
29.0
17.3
42.0
28.6
4.5
29.0
9.0
29.7
41.0
37.9
32.5
50.8
16.1
16.0
30.1
31.4
12.5
33.8
29.3
41.4
42.4
19.2
number
phases
number
622
632
635
642
645
646
650
652
655
658
660
662
666
670
673
674
675
678
679
680
681
682
683
684
685
687
689
691
692
694
695
697
702
705
706
710
711
713
717
718
723
728
730
731
734
735
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
81
latitude
time
date
23
23
23
23
23
23
23
23
23
23
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
24
25
25
25
25
25
25
25
25
25
0
4
7
13
14
16
20
17
20
23
1
1
3
5
6
7
6
9
9
10
10
11
11
11
11
12
14
15
15
15
16
17
20
22
22
23
23
0
1
2
7
15
14
13
17
17
12
37
45
57
15
48
25
29
32
58
50
15
25
33
0
45
57
15
47
8
22
6
15
35
16
41
12
27
28
36
6
57
27
9
15
57
9
12
5
26
51
38
7
6
3
8
23.3
18.8
34.8
23.0
37.7
46.0
6.9
8.7
17.6
44.6
47.3
55.9
53.6
46.5
60.5
16.8
23.5
9.2
47.5
15.2
54.8
15.8
42.1
42.3
31.0
57.8
45.8
1.9
24.9
39.8
38.7
58.9
21.5
40.0
23.8
55.5
31.7
26.1
33.8
2.9
29.5
46.0
52.2
53.5
28.9
47.6
15.85
16.43
16.66
16.02
16.73
16.81
15.48
16.05
16.60
16.17
16.13
16.77
16.26
16.69
16.83
16.05
16.44
16.71
16.63
16.74
16.47
16.37
16.61
15.59
16.30
16.14
16.41
16.12
16.47
16.51
15.30
16.89
16.37
16.13
16.14
15.78
16.16
16.26
17.32
16.17
16.03
15.83
15.95
16.71
15.98
15.96
longitude
71.60
71.82
72.49
72.48
72.51
72.45
72.12
73.51
72.38
71.91
70.08
72.49
72.85
72.58
71.55
72.38
71.82
71.61
72.73
72.34
72.45
72.65
72.32
70.40
71.98
71.71
71.98
73.43
72.28
72.14
71.87
72.50
71.88
71.68
71.66
70.84
72.47
72.23
72.02
73.02
72.40
72.68
72.37
72.32
72.36
72.37
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
depth
(km)
magnitude
RMS
GAP
(deg)
DMIN
(km)
number
phases
122.9
14.3
38.9
81.4
58.0
41.4
112.0
68.6
30.8
99.8
257.4
56.3
86.6
58.0
42.3
96.0
22.1
37.8
58.3
66.5
84.0
66.6
72.5
255.8
22.9
127.0
27.1
58.1
27.6
26.2
123.6
30.9
29.7
23.7
25.5
204.4
95.2
87.7
40.5
68.9
98.8
97.9
112.0
43.1
14.4
18.4
3.6
0.155
0.069
0.121
0.092
0.046
0.244
0.284
0.121
0.403
0.078
0.156
0.066
0.383
0.401
0.186
0.093
0.121
0.083
0.154
0.201
0.166
0.044
0.315
0.179
0.117
0.272
0.072
0. 104
0.148
0.030
0.201
0.049
0.102
0.056
0.042
0.191
0.219
0.035
0.266
0.205
0.219
0.271
0.187
0.144
0.212
0.234
96
251
226
186
247
209
146
242
156
122
299
206
152
244
218
259
216
214
263
162
122
156
131
292
187
76
130
229
124
210
144
265
120
125
133
267
93
173
278
203
160
118
114
231
176
184
12.3
9.8
26.2
35.7
28.0
38.6
51.8
29.1
30.9
13.2
137.8
32.6
36.5
19.9
24.6
33.9
11.3
34.2
7.2
42.5
13.9
19.6
34.0
102.7
10.5
25.1
10.5
36.9
25.0
22.3
20.0
43.0
11.6
27.0
26.4
64.3
20.3
16.2
34.4
55.8
34.7
10.2
12.5
44.3
14.6
13.2
17
2.7
3.0
2.4
3.5
3.1
2.8
5.7
2.7
3.3
3.1
2.5
2.6
2.2
2.4
2.7
3.1
2.8
2.7
3.3
2.5
3.9
2.1
3.2
2.7
2.0
4.4
2.9
2.0
2.3
2.5
3.0
2.8
3.2
2.6
3.3
3.3
3.8
2.7
2.1
2.1
8
12
11
1
19
22
17
24
11
28
12
24
19
13
10
12
11
11
23
20
11
28
17
10
23
8
12
18
8
27
14
10
8
8
18
18
12
25
12
15
19
24
8
12
14
number
736
737
740
748
750
754
755
763
764
772
773
774
775
778
779
782
784
786
787
788
792
793
795
796
799
800
802
803
808
814
817
818
820
824
827
828
830
832
835
836
838
839
840
841
842
843
date
latitude
__time
51.9
28.9
12.3
26.9
14.7
24.5
2.1
25.6
16.1
3.4
19.9
56.7
22.7
37.7
13.1
8.6
48.5
7.3
47.9
40.9
49.4
62.4
2.1
57.2
10.1
12.3
43.6
59.1
31.0
12.6
26.8
10.3
42.5
28.2
21.6
32.1
1.6
10.1
13.7
18.9
33.1
56.6
48.8
3.9
5.3
38.4
16.09
15.97
16.41
16.03
15.61
16.37
16.13
15.53
15.11
16.47
16.70
16.29
16.63
16.74
16.51
16.19
16.04
15.24
16.33
16.05
16.67
17.41
16.71
16.42
16.43
16.34
16.37
16.07
16.63
16.63
15.45
14.91
16.69
16.54
16.88
16.36
16.81
15.15
16.20
16.56
16.18
16.66
16.06
16.21
15.95
16.62
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
longitude
73.62
73.03
71.95
73.16
72.15
71.77
73.08
72.33
71.35
71.76
72.56
72.22
72.65
71.56
71.61
70.68
72.92
72.53
71.94
71.68
72.56
72.33
72.57
72.33
72.33
72.01
72.18
73.10
71.75
72.22
72.14
71.93
72.53
71.66
71.53
72.39
72.71
73.44
72.06
71.73
72.04
72.69
73.44
72.84
72.01
72.63
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
V
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
depth
(km)
60.4
86.4
18.4
84.5
131.7
40.1
86.2
115.1
185.8
31.5
57.5
38.0
56.0
16.9
11.2
184.9
80.2
106.8
14.6
126.9
59.7
54.0
63.6
77.9
79.3
26.0
14.7
78.3
92.7
69.6
123.1
122.1
54.3
98.2
42.3
88.8
50.2
102.9
14.4
24.4
17.4
55.1
40.8
16.7
117.0
53.4
magnitude
3.2
2.5
2.7
4.1
2.4
2.9
3.3
4.5
2.7
2.6
1.9
2.5
3.0
4.4
3.2
3.7
1.9
4.1
2.3
2.9
3.4
2.9
3.5
1.6
1.4
3.5
3.0
2.7
3.8
4.7
2.6
2.8
2.6
2.6
2.9
4.2
2.1
2.4
1.5
2.7
3.0
1.4
3.7
2.5
RMS
0.354
0.291
0.052
0.196
0.223
0.078
0.238
0.190
0.121
0.376
0.025
0.174
0.098
0.297
0.230
0.133
0.392
0.203
0.029
0.333
0.031
0.350
0.079
0.305
0.368
0.136
0.209
0.337
0.298
0.077
0.298
0.255
0.117
0.054
0.256
0.190
0.230
0.061
0.213
0.073
0.126
0.985
0.101
0.100
0.298
0.103
GAP
(deg)
DMIN
(km)
266
140
94
168
186
221
171
212
306
177
248
140
244
230
119
308
136
224
129
93
237
278
207
115
117
114
189
165
173
213
151
258
235
213
214
147
250
266
96
138
154
275
227
121
65
227
37.1
40.1
9.5
43.2
47.3
1.5
56.0
44.0
79.2
12.4
22.4
15.0
9.6
32.7
13.2
75.3
37.9
37.1
15.8
32.8
19.9
54.1
22.0
17.4
17.9
8.8
12.8
50.4
24.3
34.3
51.3
28.4
24.3
23.6
21.7
8.7
27.3
70.4
4.1
22.6
1.1
11.0
30.2
3.9
24.8
10.6
number
phases
17
16
15
12
24
12
16
17
10
19
10
12
11
16
21
14
17
19
8
27
12
16
20
24
38
10
8
22
18
10
23
26
12
10
18
12
21
13
16
20
8
14
18
8
30
16
number _date_
849
853
859
860
864
866
868
874
875
878
882
884
887
890
894
897
902
905
907
919
911
913
921
929
930
931
933
934
939
941
942
944
947
948
966
968
977
983
992
994
997
998
1081
1004
1006
10087
time_
35.7
18.3
3.0
34.0
59.0
49.2
20.0
36.1
21.1
3.5
5.7
50.8
56.4
36.2
5.5
34.1
25.7
30.0
59.4
0.9
59.3
52.5
18.7
17.6
0.1
15.4
13.9
45.5
49.8
0.6
37.9
21.4
34.4
6.7
29.2
53.2
4.7
15.0
16.6
21.2
12.1
59.3
9.3
408.5
44.0
12.9
latitude
16.73
15.30
16.56
15.11
16.57
15.43
16.96
16.55
16.17
16.22
16.15
16.68
16.09
17.22
15.89
16.39
16.34
15.95
16.67
15.58
16.59
16.63
16.39
15.85
16.21
16.83
16.51
16.03
16.25
16.19
16.63
15.54
16.06
16.39
15.28
16.06
16.38
14.86
16.46
16.08
16.15
15.88
16.44
16.48
15.47
16.38
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
longitude
depth
(km)
72.53
72.11
72.48
72.91
71.72
71.80
72.98
72.50
72.65
72.01
72.58
72.71
72.33
72.51
73.28
71.98
72.02
71.69
71.60
73.26
72.40
72.34
71.61
72.93
72.67
71.37
71.65
73.18
72.03
72.42
71.45
72.65
72.53
72.36
71.89
73.16
72.04
72.46
71.79
72.11
72.28
72.10
71.77
71.88
71.71
72.58
60.2
119.9
46.0
105.8
23.6
129.4
30.2
40.9
78.9
15.0
80.4
52.5
109.8
26.6
91.3
30.9
31.6
139.9
30.7
98.4
46.7
43.5
25.4
100.6
90.2
77.5
27.9
84.6
97.6
101.4
26.8
112.9
110.5
192.9
129.0
84.3
27.6
112.1
30.3
102.0
97.4
121.1
16.1
40.5
143.1
76.5
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
magnitude
2.3
3.7
2.2
3.8
3.9
3.5
2.4
2.8
1.3
2.7
3.4
2.7
3.0
2.7
2.2
1.9
3.9
2.3
3.8
2.6
2.2
2.5
3.8
2.8
3.1
2.5
4.2
3.0
3.6
3.1
3.5
3.5
3.6
3.4
2.0
4.2
2.1
3.0
2.9
3.1
1.6
2.4
4.1
3.1
RMS
0.025
0.448
0.030
0.206
0.172
0.296
0.172
0.147
0.132
0.079
0.061
0.193
0.033
0.215
0.053
0.987
0.157
0.258
0.138
0.167
0.293
0.177
0.128
0.338
0.467
0.147
0.116
0.302
0.244
0.278
0.089
0.186
0.399
0.451
0.320
0.241
0.041
0.233
0.069
8.150
0.059
0.099
0.104
0.113
0.384
0.218
GAP
(deg)
266
169
130
232
186
111
244
192
155
154
159
203
155
251
158
100
119
71
219
206
153
210
247
113
112
277
150
170
119
75
278
243
87
94
170
173
139
245
294
179
168
183
258
219
114
89
DMIN
(km)
26.4
38.7
23.9
46.8
23.7
32.3
52.3
22.7
26.8
5.5
24.0
12.7
31.5
54.4
24.0
12.2
17.6
21.8
38.5
32.2
28.6
35.1
17.7
24.1
25.4
38.0
21.8
41.0
7.9
17.8
45.8
24.8
32.2
12.3
18.9
45.1
16.8
76.8
13.8
13.1
26.1
34.0
10.0
5.7
38.2
12.1
number
phases
12
22
8
26
18
25
28
12
13
8
14
30
1
27
8
14
8
23
12
22
17
10
8
27
16
14
20
27
16
25
10
13
21
23
15
20
8
20
8
13
12
12
8
11
19
22
number _date
1009
1011
1012
1013
1016
1026
1027
1030
1031
1032
1033
1039
1041
1042
1046
1047
1049
1051
1853
1059
1060
1064
1065
1067
1071
1072
1073
1074
1078
1089
1090
1091
1093
1096
1097
1099
1103
1104
1105
1108
1110
1119
1125
1127
1178
1129
time
48.5
43.8
45.8
21.1
20.4
29.6
35.2
43.4
57.1
44.0
58.0
55.3
21.1
51.0
39.2
30.6
36.7
9.7
30.1
27.6
2.2
17.2
16.1
2.6
56.3
4.9
37.8
38.1
0.4
33.5
42.8
4 .5
3.3
4 .7
17.7
42.6
27.3
23.5
20.9
17.6
33.2
50.5
42.2
25.7
38.3
latitude
longitude
depth
(km)
magnitude
16.45
16.34
15.26
17.04
16.14
16.49
16.25
16.44
16.12
16.14
16.02
16.67
16.04
15.86
15.84
16.29
15.63
16.42
16.64
16.73
16.39
16.60
16.17
16.25
16.81
15.77
16.39
16.33
16.53
15.77
16.08
15.46
16.68
16.99
16.71
16.41
16.36
15.31
16.75
16.66
16.52
15.38
16.93
16.11
16.78
17.10
72.01 W
93.9
92.3
109.0
89.8
42.4
12.4
99.0
26.3
44.2
133.2
74.8
61.9
121.7
117.5
123.0
29.5
188.6
27.0
55.0
38.6
27.1
82.2
13.8
91.3
48.8
90.0
22.9
32.2
47.7
116.3
133.0
100.1
59.8
145.1
56.1
80.5
226.6
134.0
54.8
74.4
15.6
105.5
111.7
37.6
83.8
33.5
3.0
2.9
4.1
3.9
2.4
72.48
72.56
71.69
72.70
71.58
71.87
71.76
72.81
71.67
73.56
72.57
71.74
72.03
72.21
72.11
70.95
71.71
72.71
73.14
72.08
72.28
71.83
72.51
72.77
73.16
71.75
71.93
71.29
72.54
71.61
73.28
72.59
70.60
72.59
72.35
70.13
71.97
72.51
72.81
71.66
73.19
71.01
72.65
71.84
72.89
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
3.0
2.1
2.6
4.3
3.3
2.5
3.7
4.1
3.6
1.9
4.5
2.0
3.0
3.3
2.8
3.7
3.2
2.8
3.5
1.9
2.1
3.1
3.5
4.1
2.9
4.3
2.7
3.7
4.9
4.0
2.7
3.0
2.8
2.7
3.0
4.4
RMS
0.213
0.291
0.440
0.329
0.064
0.291
0.221
0.059
0.203
0.374
0.231
0.146
0.147
0.348
0.392
0.157
0.109
f.036
0.081
0.401
0.188
0.249
0.230
0.376
0.134
0.355
f0.086
0.092
0.048
0.096
0.147
0.113
0.034
0.214
.f.108
%0.286
0.079
0.072
0.016
.r.071
0.102
0.168
0.297
l1.113
0.163
0.235
GAP
(deg)
DMIN
(km)
76
94
200
246
174
123
196
263
196
10.B
77
255
232
266
80
87
154
265
294
246
236
77
122
93
85
308
149
291
211
283
226
157
227
263
295
267
113
299
263
271
251
111
251
284
160
188
251
1.2
33.1
3.7
33.4
9.7
15.6
10.1
41.2
26.2
27.3
18.5
34.5
35.3
29.3
3.0
43.8
9.6
8.0
49.0
10.0
35.2
21.7
11.6
27.4
33.9
22.5
16.0
52.4
16.0
25.8
41.2
18.3
114.5
20.8
14.7
137.1
59.8
30.3
14.9
19.3
49.1
70.9
30.5
33.9
62.5
number
phases
number
1135
1137
1138
1139
1145
1148
1151
1154
1158
1161
1162
1165
1170
1171
1173
1178
1179
1181
1184
1186
1188
1189
1192
1197
1210
1211
1218
1231
date
-
time,,
46.3
30.3
42.7
22.5
13.1
43.6
24.0
43.7
37.2
39.6
37.7
29.7
34.9
12.3
55.4
41.3
45.8
31.9
58.9
5.6
60.1
408.6
25.5
41.9
22.3
49.8
55.4
47.8
latitude
16.11
16.22
15.80
16.52
16.03
16.73
16.26
16.67
16.26
16.17
16.71
16.38
16.76
15.35
16.11
16.90
15.46
15.45
15.69
16.42
15.64
16.87
16.74
16.50
16.29
16.02
15.97
16.74
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
S
longitude
73.09
72.15
73.20
71.90
72.36
72.55
72.05
72.41
72.56
72.19
72.56
W
W
W
W
W
W
W
W
W
W
W
71.89 W
71.54
73.12
72.55
71.69
72.88
71.44
72.16
73.78
72.74
71.84
72.55
71.60
73.53
73.57
71.45
71.42
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
depth
(km)
magnitude
RMS
GAP
(deg)
DMIN
(km)
74.1
114.3
88.0
189.4
99.8
64.5
17.0
58.3
9.4
18.5
54.5
3.2
2.9
4.7
3.0
0.281
0.106
0.312
0.274
8.226
. 264
0.097
8.132
0.006
0.252
8.392
0.053
0.301
0.019
0.021
8.357
0.174
0.370
0.350
0.213
8.286
0.301
0.139
0.372
0.039
0.137
0.012
0.065
171
128
142
163
104
253
111
228
115
140
193
196
194
269
135
152
212
226
150
280
96
185
199
119
257
259
186
236
54.7
11.9
29.3
22.7
18.5
25.5
6.1
34.2
5.0
16.4
22.8
12.5
31.6
61.3
27.5
12.3
14.4
13.4
40.9
74.8
12.9
23.7
26.6
11.9
56.7
27.6
13.5
32.2
31.1
21.6
112.9
86.4
48.8
96.7
165.2
118.9
56.6
97.8
73.3
58.1
13.0
67.5
63.6
136.0
93.4
2.6
1.2
2.4
1.6
3.1
3.5
1.9
3.1
3.5
2.6
2.6
3.8
5.3
3.8
3.9
3.0
3.6
3.6
4.0
number
phases
HYPIT OUTPUT - Ist
INVERSION RUN
origin of cartesian coordinates
-16
0.
-72
0.
depth
0.
stirike
6;2.50
short distance conversions
one mir, lat
1.8443
km
orne min ion
1.7839
km
z tr
f .
nl
9
wfac
1.0000
neqs
396
layer
1
ires nkr
1
0
40.
70.
0ID.
130.
160.
190.
stn
are
ayo
cab
cay
cho
cr v
1lu
mo 1
or gt
pa
rat
siq
sis
tor
yan
pin
c n
rl
cr, n
yer
1
wt
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
].0
1.0
1.0
1.0
1.0
1.0
NS
pvel
5.3,
6.1~W
G.['
7.',;
-W
7. A'7
:0
1
7. kif
J10
7. '0
(
7. ilk
iI-0 7.90
1at it ude
-16
-17
-15
-16
-16
-15
-15
-16
-17
-15
--15
-15
-15
-16
-16
-16
-15
-15
-16
-15
int ,s
9
8
8
H
8
4
,I
27.:1
0.k
39. 6?
3.74
21.25
8.00
47.07
10.65
0.52
53.94
45.47
45.33
29.89
18.13
33.87
20.46
32.09
38.00
29.62
36.40
EW
ints
13
11
11
10
I0
5
5
swtfac
8.00
vthet
50.000
fasn
twgt
0
0
nmin kfirst
30
0
depth
-5. ('0
5. J2
20. j rh
F.
4l=
wsum
1.000
svel
3.00
3.50
3.90
4.10
4.40
4.30
4.60
4.60)
4.60
p/s
1.77
1.74
1.74
1.76
1.75
1.84
1.72
1.72
1.72
1ong Itude
-71 29.48
-71 40.31
-71 56.66
-71 22.21
-71 46.45
-71 47.71
-73 28.38
-72
2.11
-72
2.88
-72 28.39
-71 39.44
-72 43.62
-72 45.06
-72
4.85
-72 42.75
-72 28.25
-71 21.03
-71 49.69
-71 55.79
-71 57.72
P scale
1 .00
1 .00
elev
2452
240
3770
3950
1700
4500
1780
1800
50
880
4900
4000
4550
1475
140
350
4050
3700
1200
3360
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
S scale
1.00
1.00
1.00
1 .00
1. 00
1 . 110
pdelay
1.00
1.00
1.00
1.00
sdelay
flr
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
.
1.
t.
F.
F.
Yr.
f.
f.
1.
I.
1.
1.
1.
r.
1.
.
f.
psed
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
5.30
ssed
dx
dy
3.00
-20.28
71.79
3.00
-83.33
82.77
3.00
36.10 -12.06
3.00
25.00
62.96
3.00
-23.62
39.50
3.00
95.23
-24.75
3.00
-51.72 -151.00
3.00
-19.16
5.73
3.00 -101.36
47.01
3.00
-13.48
-50.11
3.00
40.73
20.20
3.00
-11.97
-81.60
3.00
12.05
-97.12
3.00
-33.65
7.78
3.00
-90.52
-38.61
3.00
-56.70
-27.20
3.00
77.83
38.04
3.00
44.50
-2.39
3.00
-45.00
31.87
3.00
40.49
-16.48
dz
-2.45
-0.24
-3.77
-3.95
-1.70
-4.50
-1.78
-1.80
-0.05
-0.88
-4.90
-4.00
-4.55
-1.48
-0.14
-0.35
-4.05
-3.70
-1.20
-3.36
-75.00
-165.40
EW vectors
-220.00 -110.00
3
NS vectors
-165.00
-82.50
EW vectors
-110.00
-220.0fl
NS vectors
-82.50
-165.:I0
Ul vectors
i:;
4
-1f.5
6
7
8
-40.00
-10.00
0.
-75.00
-55.00
-35.00
-55.00
-27.50
0.
-88.00
-66.00
-44.00
-55.20
-27.50
0.
-88.00
-66. 00
-44.00
-55.00
-27.50
0.
27.50
-88.00
-66.00
-44.00
-22.00
-55.00
-27.50
0.
27.50
-88.00
-66.00
-44.00
-22.00
1.00
-82.i0
vectors
N
-82.50
-165.0o
EW vectors
-220.00 -110.00
NS vectors
-55.00
-165.00
EW vectors
-220.00 -110.00
55.00
0.
NS vectors
-55.00
-165.00
EW vectors
-?20.00 -110.00
0.
55.00
0.
-220.00 -110.00
NS vectors
-55.00
-165.00
EW vectors
-220.00 -110.00
=
-10.00
27.50
55.00
396
55.00
0.
nvar =
scale fActors
p scale
layor
1.000
1.OOAJ
1.001
820
s scale
l.000
1.0 0
1.000
220.00
165.00
110.00
220.00
165.00
110.00
220.00
165.00
110.00
kvar
35.00
-27.50
165.00
110.00
55.00
NS vectors
-55.00
-165.00
neqs
10.00
-22.00
27.50
-22.00
vectors
LW vectors
9
1.00
vectors
'0
IN
5
1.00
1.00
NS vectors
1
2
5
5
220.00
336610
0.
55.00
0.
55.00
0.
55.00
0.
55.00
0.
165.00
10.00
25.00
55.00
44.00
82.50
220.00
44.00
82.50
220.00
82.50
220.00
82.50
220.00
165.00
22.00
165.00
22.00
165.00
27.59
165.00
27.50
110.00
225.0
0
1.000
1.000
1.000
1.000
1. 000
1.000
1.000
1.000
1.000
I. BBB
3365
1.0000
2845
0.5100
6210
s observation matrix
p observation matrix
0
B
0
3090
40
£
0
0
0
106
150
0
layer
I
217
0
& 298
0
65
0 158
128
0
338
0
0
31
8 7#7
1 111
137 309
3
45
0
11
27
59
88
193
150
119
11
0
0
32
0
2
0
0
0
0
0
0
0
0
0
0
a
0
89 131
0
0
0
0
0
0
0
0
0
0
0
0
0
23
0
10
22
94
0
2
6
0
0
0
1
0
0
66 147
0
10
2 115
0
0
1 97
0
0
0
0
287
38
0
0
0
0
100
124
197
0
0
B
123
313
0
6
0
126
3
0
263
62
143
0
0
31
645
99
268
35
0
68
0
0
0
21
0
2
0
0
0
0
0
0
0
0
0
0
0
0
0
70 178
5
0
0
13
83
0
0
66 292
59
43
64 250
295 329 156
93
27
84 245 156
16
32 525 401
73
18 334 246
101
95 113
85
4
16
0
0
3
66
16
2
1
9
39
35
57
0
11
98 155
37
26
67
89
66
56
93 108 131
81 162 211 129
170 273 295 138
136 286 395 213
107 189 431 218
101 110 296 155
4
13
22
20
24
41
64
53
0
0
0
0
0
0
0
0
0
a
1
2
0
71
0
0
0
0
62
44
312 341
89
29
17
36
78
21
117 113
4
17
layer
0
1.000
1.88000
number of p arrivals
p weight
number of s arrivals
s weight
total number of arrivals
layer
0
0
0
198
13
70
69
171
270
581
363
121
0
5
5
0
0
97 129
1
0
345
49
0
0
2
220
3
0
77
2
8
98
39
27
169
12
30
448
53 122
289
49
74 115
9
96
27
100
0 "0
0
0
174
87
123
235
324
440
460
327
7
43
73
32
176
56
162
34
36
158
62
241
268 104
205
92
3
99
67
99
177
290
30~
2;.
l ,
0
8
6
6
29
55
88
69
0
0
1
19
65
45
51
44
O
B
0
0
#0
0
0
0 12
10 50
4
0
0
1
91
0
2 68
0
0
0
0
*
0
71 173 196
22
23
3
55
2
27
1
8
0
61 139 175
3 21
20
74
2
4
layer
71
33
41
63
233
260
75
61
14
87
4
146
146
196
180
253
293
167
167
42
layer
134
160
184
245
298
331
210
163
27
25
60
61
27
90
51
166
88
195 117
209 117
203 114
99
54
5
12
98
0
0 595 225
0 297
65
30
1
0
B
B
0
0
layer
48
51
72
125
164
177
167
75
8
17
85 69 62
0 84 94 70
0 61 106 92
2 46 123 143
8 100 193 154
0 92 208 135
0 48 94 132
57 81
65
12
23 19
43
11
0 72
0
0 458 143
0 217 35
0
0 21
7
B
21
138
36
0
36
93
7
0
0
0
11
0 105
0 25
0
20
51
2
8
0
0
0
0
0
1
O
0
19
34
69
16
layer
117
146
169
222
270
300
192
145
25
6
0
layer
136
135
180
159
224
267
154
150
38
5
19
97
79
78
61
98
75
& 90 105
0
62 118 127
78
2
52 137 184 110
8 105 219 190 126
99 236 174 118
0
94
0
53 109 162
77
61
91
62
14
7
12
48
23
25
layer
67
31
38
57
204
237
66
53
14
9
B
0
0
0
17
,026
41
8
34
0
21
0
5
0
0
0
0
0
1
18
5
22
45
0
8
1
14
12
27
587
blocks were hit
a total number of
elements of g are used
172578
blocks are kept for
402
a total number of
elements of 9 are used
81003
Inversion
g diagonals for z velocity model
g diagonals for p velocity model
layer
1
5.
0.
a.
5.
0.
0.2
5.
0.
3.38
0.
0.
5.
8.
0.
0.
8.70
0.21
0.
2.57
0.83
0.
0.
5.
0.
1.01
1.40
5.
0.
0.
0.93
2.59
0.
0.
0.
2.14
0.
5.
0.35
2.22
0.
5.
0.03
10.51
0.60
6.01
1.15
5.
1.67
5.
0.
5.
0.
0.
5.
8.
6.0
0.
0.
1.87
0.
0.
8.
0.
8.
0.
2.63
8.
3.64
0.
4.33
0.
0.
B.
2.36
0.33
8.58 11.29
3.56
0.
0.46
0.
0.
4.79
6.99
4.41
0.
0.
10.61
B.
1.77
1.06
7.77
12.49
18.13
15.68
4.67
0.
0.
2.94
12.55
11.14
1.88
7.14
10.58
10.19
4.39
0.
8.
3.18
0.99
0.
3.
5.
3.98
3.18
6.081
5.
0.
0.
0.
0.
0.
1.89
4.98
2.17
0.
5.
a.
0.
0.
3.
5.1
5.91
08
0.26
6.46
0.
0.
1.86
4.28 11.57
0.
3.29
3.33
3.22
a.
6.51
4.94
2.65
2.65
6.16
4.19
9.56 11.55
5.40
7.16 13.05 16.90
5.00 12.34 17.55 10.83
5.74 10.85 14.52 14.89
9.64
9.37
5.12
3.87
3.53
5.80
9.49
3.09
0.
0.
0.
0.
8.
8.92
3.78
0.97
2.05
3.22
5.96
4.87
1.78
5.
8.
8.
0.
8.
0.
2.67
4.58
4.25
0.
B.
0.
8.
0.
0.
3.12
2.18
3.18
1.64
0.
8.
layer
layer
0.
0.
0.
0.
0.
0.
8.
4.39
5.
0.
B.
0.
5.
5.
4.53
0.
0.
0.
5.
0.
3.34
8.04
0.
0.
5.
0.
1.43
1.880
5.
4.73 5.
0.
18.56
5.
8.51
0.
2.85
1.19 0.
3.35 0. ,
a.
.805
11.98
0.
5.
0.69
2.67 7.93
.
1.35
0.
0.
B.
5.
5.
5.
a.
.
5.
5.
5.
B.
0.
5.
5.
1.62
5.
5.
0.
0.
5.
8.
5.
5.
5.
5.
B.
8.72
5.
a.
a.
0.
5.
5.
5.
S.
.
8.
5.
5.
5.
5.
3.43
rl.
B.
S.
8,.
0.79
8.
3.38
5.
2
0.
5.
layer
0.
0.
0.
8.
5.
0.
6.87 14.49 B.
B.
3.28
B.
B.
5.
B.
8.
2.87 13.82
2.76 8.48 1.20 14.88
11.13 14.22 9.29 3.11
5.
4.63 17.15 9.95
8.65 22.02 13.22
5.
7.37 0.
21.80 12.11
5.13 9.45 6.07 5.73
5.
5.
a.
a.
5.
2 .03
8.
N.
8,.
0.
4.73
3.76
5.58
0.
2.
B.
B.
8.
5.
5.
2.85
2.16
5.
5.
5.
5.
5.
0.
3.21
6.52
2.87
1.74
a.
5.
5.
5.
5.
5.
5.
2.61
2.93
8.
0.
3
4
5.
5.
3.42
5.10
7.05
6.01
6.61
5.04
3.55
0.
6.46
5.18
3.34
11.69
16.00
14.33
12.85
6.44
13.12
0.
15.25 2.45
4.20 3.88
5.54 6.44
15.08 5.99
21.43 7.22
22.64 13.87
20.69 16.63
11.74 10.54
7.10 4.27
5.
0.
a.
8.
0.
A.
5.
5.
8,.
B.13
B.
8,.
8.
5.
5.
5.
5.
5.
5.
8.
B.
5.
5.
2.33
5.
8.
B.
4.53
,.
B.
1.33
4.17
3.92
6.42
5.34
8.81
8.46
4.60
2.53
4.62
2.33
5.72 10.92
9.94
1.81
0.87
layer
layer
0.
0.
2.74
5.63
8.52
8.80
9.32
4.28
5.
0.
1.89
1.92
3.32
3.89
5.23
4.58
4.21
4.25
0.
0.
1.34
2.28
3.89
3.90
3.94
5.
4.02 10.44 16.28 11.56
9.93 17.88 12.23
3.46
8.26 12.46 15.04
1.65
7.20
9.74
7.91
2.19
0.
5.
1.27
0.
5.
5.
5.
0.
1.96
3.73
3.77
4.25
2.92
0.
5.
2.91
4.52
2.74
5.
B.
1.46 4.58
1.12
4.80
1.34 8.42
3.45 7.05
5.13 12.0
4.21 12.71
2.59 11.57
2.74 8.95
1.48
0.
6.39
11.20
11.12
14.63
19.86
20.68
16.74
15.95
f.
1.65
0.84
5.80
1.02
1.63
1.28
5.61
1.28
0.
2.82
1.81
2.88
4.19
5.95
5.98
3.67
3.55
1.56
2.95
5.
0.76
1.41
2.38
2.57
1.75
1.97
2.14
0.
5.
5.
1.05
0.57
0.53
0.63
0.88
0..66
0.38
0.96
0.
2.07
1.51
2.28
3.11
5.07
4.97
2.82
2.68
1.42
0.27
4.27
5.80
0.85
0.
1.75
2.54
0.
8.27
6.28
6.85
a.
0.
2.43
2.47
0.
0.
0.
2.51
1.05
l.
8.22
1.47
0.
5.
5.
2.81
a.
a.
5.
0.95
0.
0.
S.
0.78
0.
0.
2.19
2.59
4.25
5.94
5.92
6.36
6.69
4.53
0.
6
5.
8
5.
5.
8.59
5.
0.67
0.
layer 9
5.
5.
5.71
nvar,
5.
5.
5.
B.
3.
2.12
2.89
4.24
6.12
6.68
6.43
6.42
5.68
0.
1.11
1.73
2.62
2.99
4.30
3.48
3.58
3.29
H.
5.
4.95
1.81
2.82
5.
5.
a.
0.
5.
8.
3.69
a.
5.
5.
5
layer 7
layer
18.20
12.00
13.84
16.47
7.77
5.
5.
5.
5.
3.33
7.77
6.87
6.54
5.
5.
5.84
2.79
trnk,
ter,
are
residual norm
sLtndard variance
402
482
a
1010.85798
0.17391
5.
1.72
3.42
3.12
3.84
5.
5.
5.
8.
5.
1.19
2.06
2.43
a.
a.
8.
8.
0
0
S
0
variance
0.17391
rc: idu:: 1 variance
f0.07247
m.: re idual norm
994..3403
m.: st::ndard variance
0. '3475
0..'3 547
mo. or ,jinal variance
nv-,
t
idual variance
0. 9599
petrct eii-ge improvement
58. 30k1
'
59.23454
macr per ,entage improvement
originil
velocities for p velocity model
lay-r
velocities for s velocity model
1
0.
5.56
y.
IS.
5.45
0.
0.
0.
5.56
5.10
5.17
0.
5.50
0.
0.
0.
4.59
0.
0.
0.
90.
5.
3.29
0.
0.
0.
0.
5.
0.
B.
0.
0.
3.23
30.
2.93
2.89
0.
0.
0.
0.
3.02
0.
0.
0.
2.91
0.
0.
B.
0.
0.
B.
0.
0.
0.
3.41
0.
5.36
0.
0.5
0.
0.
r,.48
0.
G0.
0.
0.
0.
0.
0.
1.
B.
5.23
B.
5.39
3.07
3.09
0.
5.11
0.
3.43
0.
0.
0.
0.
0.
3.02
3.77
0.
0.
8.
3.07
0.
0.
0.
3.15
0.
.
0.
.r.
5.49
4.26
5.96
0.
5.96
6.
0.
0.
0.
0.
6.14
0.37
,8
0
6.13
5.
5.
0.
0.
0B.
4.98
3.33
2.93
3.35
0.
0.
0.
B.
2.95
4.93
0.
0.
3.17
0.
3.34
0.
0.
2.93
0.
B.
0r.
0.
0.
0.
0.
0.
0.
0.
5.
5.
0.5
5.66
5.9
5.92
5.96
6.12
6.01
0.
6.28
5.82
I.8W 6.0r4
6.53
5. ,9
6.49
3.57
4.92
0.
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HYPIT OUTPUT - 2nd
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origin of cartesian coordinates
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short distance conversions
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1.8443
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latitude
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1.72
1.75
1.73
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longitude
-71 29.48
-71 40.31
-71 56.66
-71 22.21
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P scale
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3770
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1780
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1
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0 298 131
0
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30, 551 107
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363 258
3GI.f 424 91
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341 106
18
52
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0
15
23
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172
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139
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323
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333 260
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0
572 blocks were hit
a total number of
elements of g are used
162078
blocks are kept for Inversion
423
a total number of
elements of g are used
89676
g diagonals for a velocity model
g diagonals for p velocity model
1
layer
0.
0.
0.
8.
0.
0.
0.
0.
0.35
0.
4.56
0.33
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2.66
0.
0.
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5.34
6.85
2.79
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0.76
1.61
1.32
3.64
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1.35
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2.53
4.55
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4.71
1.23
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2.67
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0.75
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2.48
6.21
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1.19
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2.089
3.02
4.35
4.31
2.33
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0.
0.
0.
8.
0.
0.
0.99
0.
2.38
3.61
5.61
6.01
6.30
1.65
0.96
3.27
3.54
3.86
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9.30
2.41
0.
7.79
5.91
1.14
0.
0.23
14.89
0.
1.72
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0.
11.34
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2.78
0.14 10.58
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14.41 14.68
7.80 12.37
1.28
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0.44
5.16
4.20 19.87
6.47
1.71
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0.80
0.
0.
0.88
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1.
3.84
ry.
4.
1
0.
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1.39
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0.
5.04
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0.67
6.67
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3.25
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0.30
6.28
2.21
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1.68
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1.94
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0.88
1.71
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6.61
3.17
3.30
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layer 3
1.36 10.70
2.92
2.43
2.77
4.82
8.20 14.24
14.37 14.04
10.64 17.18
9.34 14.60
7.13
5.77
7.82
7.90
0.39
0.50
5.48
3.45
7.50
6.70
13.02
15.99
16.90
11.44
3.79
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2.31
2.00
3.84
2.21
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2.82 15.42 6.71
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3.91
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3.01
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8.66 4.15
9.79 18.09 8.56
3.70
15.37 17.64 17.22
2.96
11.78 20.81 20.96
6.08
10.87 20.28 20.81 10.72
9.16
6.86 14.32
5.75
5.33
2.70
10.84 8.12
0.53
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0.
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1.82
2.54
1.89
2.79
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4.47
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0.
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1.74
1.58
1.75
0.75
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layer 4
I.
!
4.01
2.01
3.81
7.83
9.83
9.98
15. 4
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5.22 4.76
5.78
6.69
6.15
8.84
9.27 11.13
1 .89 13.24
2.99
2.02
3.51
4.14
13
1
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6.06
8.86
11.59
13.21
15.39
18.64
14.17
5.63
4.14
7.12
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3.31
13.10
6.22
15.35 10.18
18.75 9.96
17.39 11.56
0.
08.
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2.608 0.
4.28
1.68
4.21
2.59
3.78
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1.61
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4.28
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10.93
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0.
0.
0.
0.
0.
0.
1.40
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2.53
2.47
3.71
4.54
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6.18
5.87
4.75
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1.009
1.94
2.79
4.25
4.25
4.29
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3.41
0.
0.
0.73
1.71
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1.52
1.88
2.68
2.47
1 .38
1.62
1.16
2.36
2.08
3.01
5.32
5.91
5.70
4.86
3.89
1.77
0.28
0.25
4.65
3.71
0.39
0.
9.63
4.44
3.84
0.
0.
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0.36
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.
0.14
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6.85
0.
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2.30
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0.
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0.08
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12.89
2.30
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0.10
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2.32
1.96
1.48
2.33
2.80
3.88
3.89
1.93
2.18
1.44
2.93
2.31
3.39
6.45
6.60
6.79
5.98
5.39
2.30
2.27
2.24
3.36
3.98
5.86
4.58
5.37
4.49
0.
0.
1.81
2.35
3.35
2.93
4.05
2.70
2.84
0.
0.
0.
0.74
5.54
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0.
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0.
0.35
0.
0.
0.
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0.
1.07
0.
0.
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0.72
1.92
0.
0.
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layer 5
0.63
0.
0.
0.
0.05
0.58
0.36
layer
2.78
2.99
2.16
2.14
1.92
0.
0.26
0.78
1.11
1.26
0.
0.
B.
0.88
9.34
6
4.69
layer 7
0.67
0.
layer
0.
0.
8
0.
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0.49
0.48
1.56
0.59
0.
0.
B.
B.
B.66
layer 9
0.29
nvar,
Irnk,
ter, are
423
423
0
1030.19531
residual norm
0.17738
stnndard variance
0.17802
original variance
0.07487
residual variance
988.58447
mod residual norm
0.23463
mod standard variance
0.23521
mci!1 original variance
0.09319
no, reidual variance
57.94295
poi centage improvement
improvement 60.38184
Fer.nrltage
pm:
0.
0.
1.15
0.
8.
2.39
3.02
1.80
8.98
0.
0.
0.
0.34
1.86
0.
B.
B.
0.
velocities for p velocity model
velocities for s velocity model
layer 1
5.52
0.
0.
0.
5.
B.
B.
0.
3.30
0.
a.
B.
5.
5.
B.
B.
0.
0.
0.
5.51
5.13
0.
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5.
0.
5.
0.
3.18
2.91
0.
0.
0.
0.
4.77
0.
0.
0.
0.
0.
5.
5.
2.99
0.
0.
5.35
5.44
5.30
0.
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5.30
4.94
5.38
3.04
3.36
3.04
0.
a.
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3.BS
3.11
0.
0.
4.90
5.93
0.
4.92
0.
5.
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2.97
3.27
0.
3.59
5.
5.
5.51
0.
4.33
5.76
0.
0.
5.13
5.
3.36
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2.92
3.29
5.
5.
2.96
0.
0.
5.25
0.
5.74
5.07
5.19
0.
0.
0.
3.12
0.
3.28
2.87
3.09
5.
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0.
0.
0.
0.
0.
0.
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0.
0.
0.
0.
0.
0.
0.
0.
5.
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6.74
5.90
0.
0.
0.
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3.65
5.
5.
5.
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5.
0.
0.
6.20
5.81
0.
0.
0.
5.
0.
3.53
3.50
0.
5.
5.
0.
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6.05
5.83
0.
0.
0.
0.
0.
3.64
3.47
0.
5.
5.
6.54
6.20
6.04
5.93
0.
0.
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3.95
3.48
3.53
3.51
0.
5.
5.
6.01
6.30
5.80
0.
0.
0.
6.58
3.78
3.75
3.56
0.
0.
5.
3.32
6.00
6.03
6.24
6.04
6.05
0.
5.93
3.50
3.69
3.65
3.48
5.
0.
0.
6.05
5.91
0.
a.
3.62
3.62
3.46
3.45
0.
5.
5.
layer 2
6.41
6.21
6.13
5.94
6.30
5.76
6.52
5.86
5.98
5.80
6.24
3.82
3.51
3.67
3.39
3.50
3.45
3.72
6.05
6.25
6.18
5.56
5.92
0.
0.
3.69
3.46
3.66
3.44
3.75
5.
0.
6.23
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
0.
6.84
7.95
7.16
6.71
0.
0.
4.11
4.69
4.16
0.
0.
0.
5.
7.22
7.40
6.87
6.53
0.
0.
4.24
4.33
4.01
3.71
0.
0.
5.
7.16
7.36
6.60
6.20
6.22
0.
4.00
4.04
3.73
3.78
0.
0.
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layer 3
7.'1
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7.0"
6.16
7.4r
7.
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6.26
0.
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0.
4.03
3.97
3.91
3.83
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6.98
4.01
4.24
4.02
3.78
0.
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3.76
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6.11
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0.31
6.46
4.09
4.05
3.96
3.79
3.79
0.
0.
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6.67
6.17
6.37
G.61
6.46
4.13
3.87
3.90
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3.57
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0.
7.31
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6.67
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6.52
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3.92
3.91
3.85
3.78
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6.76
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3.88
3.92
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0.
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4.09
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7.41
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4.57
4.50
4.20
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7.74
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6.81
6.74
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0.
4.28
4.51
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0.
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7.73
7.74
7.33
6.8
6.84
6.91
0.
4.31
4.39
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3.96
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6.95
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7.78
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6.44
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3.87
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7.76
7.18
6.60
7.05
6.81
6.86
4.49
4.47
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3.86
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7.44
7.32
7.43
6.72
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6.81
0.
4.29
4.24
4.22
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0.
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7.30
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0.
0.
0.
0.
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4.18
0.
0.
0.
0.
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8.12
7.80
7.67
7.78
7.76
0.
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4.35
4.45
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7.84
7.93
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7.47
7.62
7.60
0.
4.45
4.44
4.50
4.49
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0.
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7.88
7.93
7.91
7.91
7.75
7.75
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4.60
4.57
4.61
4.55
4.53
4.37
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7.64
7.72
7.80
7.55
7.62
7.58
0.
4.65
4.53
4.52
4.35
4.37
4.39
7.60
7.65
7.84
7.77
7.57
7.74
7.73
4.56
4.61
4.54
4.60
4.46
4.35
4.13
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7.81
8.04
8.02
8.01
7.79
0.
0.
4.34
4.66
4.45
4.40
4.48
0.
7.0
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8.16
7.9F
7.90
7.99
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4.65
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7.65
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7.53
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4.39
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4.75
4.31
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layer
5
0
7.50
7.69
0.
0.
7.52
0.
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7.73
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0.
7.58
0.
0.
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4.33
4.52
4.58
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4.43
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7.80
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4.25
4.74
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8.21
8.19
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layer
layer
0.
layer
0.
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0.
7.93
4.63
0.
8.00
4.50
70.
0.
0.
0.
4.64
7.84
%frnction
change for p velocity model
Xfraction change for
s velocity model
.3
oil3
.3
.3
.3
.3
8L '3
3),*v
9)v
96*S
L99S.3*
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0.16
0.14
0.
0.
0.09
0.08
0.
0.
0.
0.
0.
0.
0.
0.
0.
layer
.A
.
8
0.
0.
b.
0.
0.
0.12
0.
0.08
0.
0.12
0.
0.07
B.
0.
0.
B.
B.
0.
B.07
layer 9
0.
B.
0.
.
0.10
HYPIT OUTPUT - 3rd
INVERSION RUN
origin of cartesian coordinates
-16
0.
-72
0.
depth
0.
strike
62.50
short distance conversions
one min lat
1.8443
km
one min ion
1.7839
km
wfac
1.0000
ztr
0.
nl
9
depth
-5.00
5. 00
30. J0
60. 00
80. 00
100. 00
130. 00
160. 00
190.00
4
5
7
8
9
stn
are
aye
cab
cal
cay
cho
cry
1lu
mol
ong
pat
rat
siq
sis
sgp
tor
yan
pin
C F ril
wt
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
1.0
C,0,n
layer
1
2
3
4
9
8
8
8
8
5
5
pvel
5.25
6.05
6.75
7. 10
7.70
7.90
7.90
7.90
7.90
latitude
-16 27.73
-17
0.80
-15 39.62
-16
3.74
-16 21.25
-15
8.00
-15 47.07
-16 10.65
-17
0.52
--15 53.94
-15 45.47
-15 45.33
-15 29.89
-16 18.13
-16 33.87
-16 20.46
-15 32.09
-15 38.00
-16 29.62
-15 36.40
NS int s
EW
swtfac
8.00
vthet
50.000
twgt
0
lasn
0
nmin kfirst
20
0
ires nkr
1
0
neqs
419
layer
1
wsum
1.0000
ints
9
11
11
10
6
6
svel
3.05
3.45
3.90
4.05
4.45
4.30
4.60
4.60
4.60
p/s
1.72
1.75
1.73
1.75
1.73
1.84
1.72
1.72
1.72
longitude
-71 29.48
-71 40.31
-71 56.66
-71 22.21
-71 46.45
-71 47.71
-73 28.38
-72
2.11
-72
2.88
-72 28.39
-71 39.44
-72 43.62
-72 45.06
-72
4.85
-72 42.75
-72 28.25
-71 21.03
-71 49.69
-71 55.79
-71 57.72
elev
2452
240
3770
3950
1700
4500
1780
1800
50
880
4900
4000
4550
1475
140
350
4050
3700
1200
3360
pdelay
P scale
1.00
1.00
1.00
1.00
1.00
1.00
S scale
1.00
1.00
1.00
1.00
1.00
1.00
1 . 03
1.00
sdelay
flr
F.
F.
F.
F.
F.
F.
F.
F.
Y.
F.
F.
F.
Y.
F.
F.
F.
f.
F.
F.
F.
psed
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
5.25
ssed
dx
dy
3.05 -20.28
71.79
3.05 -83.33
82.77
3.05
36.10
-12.06
3.05
25.00
62.96
39.50
3.05 -23.62
3.05
95.23
-24.75
3.05 -51.72 -151.00
3.05 -19.16
5.73
3.05 -101.36
47.01
3.05 -13.48
-50.11
40.73
3.05
20.20
3.05
-11.97
-81.60
3.05
12.05
-97.12
7.78
3.05 -33.65
3.05 -90.52
-38.61
-27.20
3.05 -56.70
3.05
77.83
38.04
3.05
44.50
-2.39
3.05 -45.00
31.87
3.05
40.49
-16.48
dz
-2.45
-0.24
-3.77
-3.95
-1.78
-4.50
-1.78
-1.80
-0.05
-5.88
-4.90
-4.00
-4.55
-1.48
-0.14
-0.35
-4.05
-3.70
-1.20
-3.36
4
4
1.0
1.00
NS vectors
1
-:65.:r0
-90.00
E 4 vccLor,
0 - 11t0. 00
-20.
-55.00
-30.00
0.
20.00
45.00
90.00
165.00
-75.00
-45.00
-10.00
25.00
55.00
110.00
220.00
-55.00
-27.50
0.
27.50
55.00
165..0
-88.:70
-66.00
-44. 00
-22.00
-55.
-27.50
0.
-- 88.00
-66.00
-44.00
-55.00
-27.rO
0.
-88.
Of
-66.00
-44.00
-55.00
-27.50
0.
N', vector-
2
-165
0
I
- ..
3
-l2.
verL,or
-rII~J
5
4
S W vector:
:" -8211.A
4 W vcctor
-88.
NS v
-165.'
r00o -GG.00
-22.00
-44.00
27.50
-22.00
27.50
-22.00
ctor5
-55..0
15 . (To
EW vector;
7
27.50
NS vectors
-165. :' -55 .10
I vectors
140..0
(I' 0 --
vcctors
8 -165 N!
.. 0
0.
85.00O 165.00
-60. 00
3 '..r O
120.00
15.00
05.00
165.00
30.X0
120.00
-60.00
165.00
I'! vectors
-12.100
9
-155.
-?
ner:v
s -
0.
55.00
0.
?2.00
44.00
82.50
220.00
44.00
82.50
220.00
82.50
220.00
82.50
220.00
165.00
22.00
V!'
v
'. r
-U'5.
6
1.00
1.00
.
-70. 00
r:s vectors
0
0.
1Md vector:;
-70.0.0
0. (0
-
220.00
165.00
70.00
764
nvar
A 19
I Lor
70..0
,
*( 1 ,-
SC'c-'
C
I .0-I
220.00
kvar -
292230
220.00
220.00
55.00
0.
55.00
0.
165.00
27.50
165.00
27.50
0•
1.000
1.00
1.00
1.000
1.000
1. 0
0
0
0
1.000
1.50
1.I00
1.00
1.50
1.000
number of p arrivals
p weight
number of s arrivals
s weight
total number of arrivals
3559
1.005B
309
0.500
6568
p observation matrix
layer
10
9
44
78
378
107
87
96
122
7
layer
76
62
87
103
332
3~6
14
8
G'
1
s observation matrix
1
0
27
S0
9
a
316 578
0
&
0
114
0 156
D
0
layer
0
0B
231
0
0
111
362
150
B
0
0
0
315 137
B
226
5
a
8
25
11
405
0 170
11
326
1
48
37 151
0
0
214
42
133
161
312
426
733
449
252
8
24
7
a
0
6
a
113 136
4
a
69
384
14
2
13
275
83
149
12
22
38
61
38
247
44
569
88 153
98 126
88
356
13
36
124 115
0
4
2
8
B0
a
B
41 151
4
0
126
8
0
a
0
0 25 209
0
5
8
B 278
S8
B9 208
303 547 98
10
8
0 324 375
107
8 138 282
0 131
0 37
a
5
72
5
5
8
5
12
0 104
2 1I
28 58
15
12
42
77
350
94
83
85
186
8
97
45
20
110
382
192
135
66
126
22
194
45
118
152
281
395
672
411
192
8
22
97
324
240
139
228
491
296
106
2
5
73
27
15
8
25
59
58
67
1
5
0
0
1
10
27
88
67
25
0
0
6
55
19
26
77
9
B
69
58
81
90
288
328
127
71
65
12
116
145
190
241
314
346
215
135
163
59
155
148
168
273
338
359
263
177
149
31
56
56
79
126
167
206
204
106
45
9
13
13
26
33
65
73
71
35
26
2
0
2
6
8
25
31
36
27
18
1
5
0
5
12
28
35
32
14
6
5
0
B
22
2
77
0
2
105
44
19
118
405
208
144
89
159
23
8
0
3
123 174
162 164
206 194
269 305
346 386
38no0 399
23' 297
161' 291
IfRc;179
G!
34
18
68
23
69
98
61
170
70
252
98
250 120
261 123
149
69
59
36
13
4
a
11
21
21
56
75
75
54
27
4
0
3
11
25
52
62
61
29
11
0
0
0
8
55
5
5
0
0
layer
50
0
1
13
23
54
14
15
30
4
108
124
89
64
117
119
87
84
37
layer
5
0
O
ff
35
49
30
30
61
18
19
46
19
k"
V
1
1
22
13
layer
82
122
146
151
205
247
148
117
43
73
77
81
78
62
98
65 151
163 150
144 126
73 125
71
68
37
12
47
66
62
85
97
95
81
69
6
0
27
68
9
0
1
7
22
39
49
46
37
21
1
47 98 75
43
0 114 110 55
1 84 133
76
13 59 141 124
23 109 185 131
54 110 227 127
13 82 132 115
13
78 105 57
28
34 40
6
22
27
29
56
76
68
47
29
1
3
8
17
34
34
33
23
18
1
1
8
16
30
29
20
9
0
17
35
69
71
71
69
50
42
5
2
29
70
67
57
35
33
28
3
0
0
0
0
0
1
1
19
13
34
43
38
56
63
65
57
47
2
13
25
51
47
43
41
25
25
1
1
15
35
40
43
24
18
12
1
31
63 61
44 67 52
30 55 72
30 61 126
56 146 122
18 128 99
17
66 107
41
64 66
15 33
9
0 34
6
0 117 111
1 334 215
12 122 67
5 20
a
0
13
41
4
B
0B
7
0
B 0
0
&
B
0
1
11
13 114
61 130
17
14
22
9
0
0
2
9
13
51
13
layer
8
0
0
0
G
51
85
layer
r
9
1
0
7
17
33
64
70
54
43
29
4
6
0
50
9
0 147 166
1 413 335
14 152 111
4
27
6
layer
5B
32
73
38
105
55
156 1I0
163 124
167 102
139
81
72
50
9
4
77
93
7
14
4
0
blocks were hit
609
a total number of
elements of g are used
:;' 745
a
blocks are kept for
465
",Lal number cf
elements of g are used
I0 .345
Inversion
g diagonals for s velocity model
g diagonals for p velocity model
layer
1
0.
0.
J.
4.14
1.
.98
0.
0.
lay.r 2
.36
r.
3.46
0.
0.
0.27
6.75
2.24
0.
0.
9.96
2.49
0.
8.24
6.23
1.2
0.
0.
5.44
0.
0.
0.
0.
0.24
0.
0.
0.
0.
0.
0.78
0.39
0.
4.89
0.
0.
0.
0.
AL.
0.
7.31
0.
2.77
0.
0.
0.
0.
0.
2.31
0.
0.
0.05
0.
1.23
0.
1.47
0.
5.04
0.
0.
4.91 0.
0.
11.72
0.
3.20
0.38
0.
8.28 10.47
2.83
8.11
0.
4.23
0.
0.
0.
0.
0.
0.
1.78
0.
0.
0.
0.32
a.
B.
0.
0.
1.40
0.
0.
0.
.
0.
6.68
0.
2.09
0.
B.
B.
0.36
0.
4.48
1.69
B.
0.
B.
0.
lay-r 2
0.81
D.
tI
1.31
3.27
4.22
7.55
10.48
10.20
7.36
4.03
2.42
0.
6.85
5.75 13.60
3.16
8.27 12.83
12.31
9.86
5.73
12.49 19.94 11.23
20.69 27.79 12.61
22.53 29.72 18.47
15.89 20.60 22.95
10.84 10.25 10.19
4.48
10.00 10.61
0.50
0.
2.21
0.
1.05
0.
1.58
0.98
1.75
2.06
3.50
5.9C 2.33
3./79
2.03
3. 01 1.91
0.
0.
0.72
1.06
1.83
1.37
1.64
1.04
0.
0.
0.
0.40
0.25
0.
16. 3,"
22.1 f
19.72
7.61
0.
2.32
9.57
7.13
8.48
0.
4.78
6.07
3.64
10.93
18.03
18.05
11.84
8.04
7.71
1.77
5.84
2.96
5.54
11.32
11.49
15.61
19.50
9.62
3.98
0.
0.
1 .29
4. 13
5.39
7.51
8.84
9.56
3.90
2.74
0.
4.56
3.36
0.
0.
0.
0.
0.
11.98
3.?? 4.11
J.99
2.33
9.26
7.22
0.
2.78
0.
3.
34.46
3.84
7.89
11.69
27.56
37.81
42.96
33.76
11.43
0.
1.06
8.41
23.36
19.74
7.94
21.10
25.28
22.02
9.80
0.
0.
2.72
1.20
0.
0.
2.60
10.42
7.56
6.99
0.
0.
0.
0.
0.
0.
2.15
B.
8.
0.
2.
10.02
0.
6.32
1.44
7.08 7.50
2.70 0.
0.
8.
3
1.44
2.39
3.56
5.96
9.51
8.73
7.53
3.77
2.55
0.
layer
i .59
1.15
3.35
4.62
5.25
4.37
2.07
f0.
0.
0.
0.
1.83
3.34
5.62
3.17
2.04
0.
0.
0.
0.26
layer
25.67
0.47
0.45
8.13
29.38
16.39
8.95
3.64
26.95
2.65
0.76
7.21
23.02
16.32
16.44
0.
0.51
5.33
14.16
5.99
2. 50
8.76
10.53
0.
B.
0.
0.76
6.11
17.22
5.94
3.87
13.12
12.40
0.
25.43
2. 97
6.58
,0.
8.91
G. 04
2,.93 22.'92
28.37
32. i4
25.91
9.99
19.59
0.
2.99
0.
10.68
9.79
7.92
15.27
21.52
24.51
15.27
8.34
9.61
9.47
£3.
0.
0.
0.
2.89
3.51
6.91
7.14
7.46
2.70
2.83
0.
B.
0.
0.
0.
1.54
1.78
3.06
3.68
0.
0.
8.
0.
0.
0.
2.96
4.50
3.39
0.
0.
0.
9.75
1.79
1.26
2.84
4.54
3.11
2.61
0.
0.
0.
1.41
1.68
1.52
1.45
0.
0.
0.
0.
1.94
1.43
1.33
4
1.66
2.31
3.43
1 .54
4.3!0
1 .4
i .2 -, 4. 90
5. ,.r
I .95/
7., 3
S.5 /
4. 46
1.48
2.46
3.46
6.
40
. 34
I'.7
2.88
1.87
2.21
1.66
;-.98
2.98
2.53
2.06
4.03
5.54
6.29
6.98
9.47
5.71
1.69
2.45
3.93
4.73
7.48
5.90
5.56
5.
a.
B.
0.
0.24
2.75
£.92
4.23
1.24
3.25
0.
2.23
0.
1.47
0.
8.84
0.
0.08
0.88
1.16
1.11
0.
9.74
1.70
2.41
2.22
2.42
1.61
1.19
0.
0.
0.38
1.87
1.64
1.47
1.082
8.96
0.74
0.
0.
0.23
3.22
0.97
5.37
1.59
3.25
0.
1.82
B.
B.
0.
B.
8.
8.89
0.16
0.05
0.27
8.31
0.
0.
0.73
0.
1.21
0.85
0.89
1.61
1.05
0.93
1.58
1.67
2.26
2.49
2.31
2.85
a.
.
0.75
1.44
2.20
1.56
2.35
8.93
0.89
0.
5.
5.
5.99
1.68
0.
0.
0.36
0.
0.
layer 5
0.
8.
0.
8.
0.
0.24
0.
layer
0.06
0.02
0.12
0.13
0.
0.
0.59
0.
0.60
0.68
0.90
2.05
1.58
1.02
1.24
0.81
1.37
1.16
2.42
3.15
3.29
3.10
3.39
2.61
0.
0.26
0.21
5.51
5.11
0.41
8.
0.76
5.10
4.44
0.
8.
0.19
0.34
0.
8.
0.13
0.23
8.10
5.94
0.56
8.
1.01
6.96
3.80
0.
0.
0.
0.
0.85
0.
0.
0.
0.
8.09
8.
0.
0.
8.
8.
1.37
0.
0.
8.
1.01
2.10
B.
1.95
2.01
2.66
3.12
2.51
2.36
0.
1.56
3.36
0.89
0.
6
layer 7
B.
0.67
2.61
0.
layer 8
0.
0.65
0.59
0.
0.
0.
5.85
0.75
layer 9
0.
0.78
0.
0.34
nvar,
1.26
2.61
2.07
1.37
irnk,
ter,
are
465
465
0
1268.84448
residual norm
0.20789
standard variance
0.28791
original variance
0.08232
residual variance
1205.84875
modI residual norm
0.27132
m,,' st.:,dard variance
0.27239
or j iriAl variance
m..
0.09925
<, du l variance
m.,.'
60.40707
-l ' (i" imp ,ovement
p.
63.56284
-, t.--ge improvement
1.21
2.66
3.35
3.72
3.07
3.49
1.37
1.82
1.
$.
velocities for
velocities for p velocity model
layer
a velocity model
I
0.
5.33
5.74
0.
0.
0.
0.
,0.
0.
5.74
5.09
0.
0.
0.
0.
3.84
3.34
0.
B.
0.
B.
0.
0.
3.39
2.91
0.
0.
0.
B.
3.00
0.
B.
5.
5.
B.
B.
B.
B.
0.
f.
4.62
0.
0.
5.
0.
5.06
5.47
0.
0.
5.27
5.01
5.37
3.27
3.33
3.15
0.
B.
3.55
3.55
g.
5.11
6.10
0.
5.00
0.
0.
0.
0.
2.99
3.26
0.
5.
B.
0.
2.88
B.
0.
5.38
J.
4.27
6.32
0.
0.
5.09
0.
3.34
0.
2.85
3.36
0.
0.
5.44
0.
5.89
4.87
5.13
0.
0.
0.
3.17
0.
3.24
2.82
3.15
0.
B.
0.
,0.
0.
0.
0.
i0.
0.
0.
0.
0.
0.
0.
B.
0.
0.
0.
6.74
7.49
6.29
0.
0.
a.
layer
2
0.
6.71
0.
.
6.80
.48
6.71
0.
4.00
4.21
3.65
0.
B.
B.
0.,
3.68
3.73
3.72
3.58
0.
B.
0.
3.71
3.76
3.67
3.52
3.41
B.
B.
0.
B.
0.
6.66
6.23
6.30
6.35
6.14
6.20
6.55
6.31
0.
0.
0.
3.96
3.74
3.69
3.59
6.56
'K.68
6.70
6.43
0.
6.06
6.18
3.80
3.90
3.81
3.66
6.61
C,.46
6.19
6.32
5.90
6.29
6.12
3.74
3.74
3.74
3.72
3.53
3.56
6.51
G.51
6.22
6.30
5.94
6.13
6.12
3.67
3.71
3.67
3.65
3.51
3.49
3.64
6.92
6.57
6.40
G.22
6.11
5.95
6.23
4.07
3.89
3.67
3.65
3.71
3.56
3.47
6.67
6.59
6.44
6.21
5.98
5.89
0.
3.86
3.74
3.73
3.71
3.61
3.55
S.
0.
6.56
0.
0.
0.
0.
0.
0.
3.81
0.
a.
B.
B.
0.
7.49
7.38
6.55
0.
0.
4.54
4.46
4.41
4.01
0.
9 t
.82
7.40
6.76
6.70
0.
4.24
4.47
4.38
3.89
'"
.74
7. '8
6.35
6.34
6 .27
4.13
4.35
4.38
3.94
layer
0.
3
7 85
7.
B.
4.00
7.71
7.44
7.40
6.64
6.49
6.71
7.01
4.21
4.25
4.31
3.91
4.02
0.
a.
7.58
7.65
7.69
6.63
6.53
6.69
6.94
4.14
4.48
4.44
3.94
3.75
3.76
3.92
7.46
7.53
7.49
6.66
6.36
6.77
6.64
4.20
4.39
4.34
3.96
3.79
3.79
3.93
7.80
7.31
7.14
6.48
6.43
6.83
6.75
4.28
4.26
4.17
3.91
3.82
3.99
4.59
7.27
7.35
6.98
6.53
6.50
6.80
6.75
4.18
4.27
4.08
3.88
3.84
3.94
a.
7.88
6.72
7.11
6.41
6.68
G.52
0.
4.29
4.08
4.04
3.75
3.99
0.
B.
0.
7.47
6.85
0.
0.
£.
0.
0.
4.42
3.85
0.
0.
0.
0.
7.63
7.69
7. 59
7.32
7.33
0.
0.
4.47
4.38
4.41
4.04
4.17
0.
0.
0.
7.54
7.47
7.34
7.21
0.
0.
0.
4.36
4.29
4.31
4.25
0.
0.
0.
7.75
7.70
7.72
7.15
7.46
7.33
0.
4.56
4.33
4.42
4.17
0.
0.
0.
7.76
7.44
7.50
7.19
7.09
7.32
0.
4.43
4.24
4.38
4.19
4.23
0.
7.78
7.74
7.54
7.40
7.18
7.20
7.18
4.32
4.57
4.40
4.33
4.27
4.03
4.03
7.12
7.74
7.G65
7.65
7.18
7.24
7.20
4.48
4.42
4.48
4.41
4.12
4.17
4.09
0.
7.63
7.71
7.55
7.28
7.30
7.48
0.
4.43
4.38
4.38
4.11
4.09
4.19
layer
4
0.
7.63
7.58
7.45
7.16
7.39
7.17
0.
4.47
4.38
4.35
3.89
0.
0.
7.92
7.56
6.95
0.
0.
0.
0.
4.57
4.25
4.10
0.
0.
0.
0.
7.76
7.65
7.55
7.65
0.
0.
4.43
4.47
4.48
4.43
0.
B.
layer
5
0.
7.93
7.78
7.82
7.56
7.35
7.60
4.51
4.52
4.34
4.50
4.33
0.
0.
0.
7.81
7.54
7.92
8.20
7.93
7.44
4.48
4.60
4.57
4.49
4.56
4.35
0.
7.35
7.18
7.61
7.98
7.65
7.68
4.86
4.43
4.45
4.60
4.14
4.41
7.50
7.57
7.80
7.70
7.81
8.05
4.67
4.50
4.54
4.44
4.51
4.25
0.
7.85
7.85
7.99
7.95
7.85
0.
4.49
4.59
4.28
4.41
4.46
7.76
8.04
7.66
7.98
7.50
0.
4.87
4.82
4.35
4.28
0.
7.97
7.90
7.66
7.62
7.76
4.48
4.69
4.61
4.24
4.31
0.
8.42
.4?
0.
0.
7.29
H.
7.65
0.
7.71
H.
0.
0.
0.
0.
4.12
0.
4.42
0.
0.
7.75
8.40
4.18
4.76
0.
8.16
8.33
7.62
4.51
4.57
4.62
8.16
8.14
0.
4.43
4.41
0.
3 ..
92
0.
0.
4.33
0.
0.
f0.
0.
0.
0.
0.
0.
0.
0.
0.
7.82
8.34
7.89
0.
4.62
4.52
0.
0.
0.
0.
0.
0.
0.
0.
layer
0.
G.
1ayer
0.
g0.
0.
0.
4.90
layer
0.
0.
9.
0.
B.
7.93
4.57
I11.,9
4.52
0.
4.
0.
7.87
Xfriction change for p velocity model
4.71
Xfraction change for a
velocity model
layer
1
0.
0.
0.
0.
0.
0.
0.
5.
8.
0.
0.
0.
1.51
5.13
-1.94
8.53
0.
0.34
0.
5.
-6.64
11.85
0.
0.
-3.83
5.
0.
0.
12.93 -2.89
0.
0.
0.
0.
-0.06
3.18
5.49
7.43
3.29
0.
0.
0.
0.
7.70
0.
0.
0.
2.33
0.
7.87 -6.14
3.33
5.
B.
0.
0.
0.
0.
0.
a.
a.
5.
-19.46 21.54
0.
0.
0.
0.
-3.91
J.
0.
0.
0.
0.
5.
0.
17.27
0.
5.
0.
1.41
0.66
0.
0.
0.
0.
b.
0.
0.
3.24
5.
0.
0 .
-3.60
0.
-0.38
10.34 -2.13
5.
B.
0.
9.36
-2.07
0.
0.
0.
0.
0.
-11.14
-5.40
-6.25
0.
8.36
-1.25
0.
13.33 -6.30 -1.33
.
-3.72
0.
-2.07
0.
0.
0.
0.
0.67
0
0.
0.
a.
0.
B.
0.
0.
0.
0.
0.
.
B.
layer 2
P.
4.51
f.
4.04
5.75 -0.29
1.68
1.46
0.
0.72 -1.68
-0.01
18.93
8.15 17.00
1.45
f.
0.
a.
-0.44
3.68
3.22
0.79
0.
0.
-3.76
1.71
1.81
-2.09
-3.84
B.
0.
2.87
0.97
2.46 -0.32
0.
0.
0.
-1.35
5.38
5.83
1.74
0.
0.
1.46 -1.25
-2.75
1.01
3.88
3.45 -0.56
-1.31
-4.59
0.17
1.92
1.36 -1.01
0.43
5.73
5.12
2.02
1.28
4.59
0.22 -2.32
0.
0.23
1.07
3.53
3.13
1.80
0.01
0.
0.
0.
0.
0.
a.
2.98
0.
0.
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0.
0.
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0.13
Y.51
3.89
0.95
0.
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3.54
6.30
2.83
0.
-1.41
0.09
1.51
1.19 -4.89
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0.90
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3.30
1.78
1.67 -0.50
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2.11
2.16 -0.64 -3.50 -5.06
1.64
0.
3.33
3.33
5.44
-4.00
7.85
5.77 -1.27
-0.79
-1.42
6.71
3.93 -7.34
-6.03 -6.45
1.41
2.65
5.69 -3.00 -3.79
0.
layer
-i.f -
-2.18
9.72 -4.24 -1.17
-1.52
-4.00
-0.27
0.34
-1.81
-1.34
0.
2.40
0.
0.
0.
0.
3.02
0.
0.
0.
4.42
7.37
0.
0.
-2.61
7.73
9.39 -0.18
0.
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4.87
9.46
1.08
2.48
0.
a.
0.09
4.70
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3.62
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7.92 11.08
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3
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9.82
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10.32
1.00 -3.81
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1.93
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3.82
6.93 -2.77
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0.98 -0.84
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5.67
8.53
1.51
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2.G66
0.82
2.00 -5.39
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1.96
9.82
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2.55
4.32
0.28 -2.17
3.51
6.34
1.40 -0.27 -4.71
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1.55
0.72
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2.89
2.02 -0.40 -1.41
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5.
0.
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-1.77
0.99 -3.78
2.38
0.
B.
0.
0.
9.
-4.35
3.64
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0.
layer
1.54 -6.47
3.08 -2.13
0.
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2.53
0.
0.
0.
0.
6.50 -3.78
1.16
(.
0.
8.35
0.77
3.68 -3.78 -0.67
0.
1.
0.
4
-1.59
1.19
1.89 -0.35
0.
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0.21
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0.
0.
0.
0.24
0.89
2.60
1.11
B.
0.
0.
2.04
3.32
5.01
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2.99
1.13
0.
4.76
1.98
5.27 -0.73
0.
B.
0.
2.09 -0.07
2.08 -0.81 -2.18
0.91
0.
1.84 -0.31
4.19 -2.27
1.92
0.
0.39
1.88
1.23
0.70 -1.03
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4.99
3.63
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4.10 -0.99 -0.13 -0.73
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0.
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3.49
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0.63
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0.
1.89
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0.98
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1.41 -1.25
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2.68
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3.56 -7.42
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0.
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0.
2.64 -2.28
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.
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0.
0.
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1.23
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1.70 -2.77
0
0. .
1.42
0.67
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0.48 -1.55
layer 5
0.
0.14 -0.62 -1.94
0.
2.28
0.
0.84 -2.04
1.06
-0.67
1.60 -1.77
2.88.
0.
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0.
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1.34
2.29 -1.79
2.20 -1.67
3.94 -3.41
0.73
4.06
3.35
2.10
3.74
-1.85
3.70 -0.71 -0.23
9.23
0.29
0.71
4.51
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0.27
0.97
-1.62
1.24
0.04
1.41
4.56
5.03
1.81
2.62
3.73
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1.97
0.
1.48
3.87
3.70 -2.54
0.
10.22
0.
0.
1.91
1.98
0.
0.
0.73
4.37 -0.50
3.50
2.60 -0.53 -1.07
7.90 -1.09
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0.
0.
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6.47
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0.
0.
0.77
0.67
0.
0.
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2.49 -3.48
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0.31
9.02 -1.17
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0.
4.30 -3.57
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0.
0.
0.
0.
1.43
0.
layer
0.
-3.16
0.
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0.
0.
0.
-1.96
2.71
0.
0.
0.
6.39
-2.87
10.70
3.34
5.50 -3.59
4.91
6.19
7.36
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3.34
3.01
0.
3.01
2.50
0.
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1 .51
0.
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0.60
0.
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layer
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0.
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7
-0.97
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5.62
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0.48 -1.
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0.
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fres
0.
0.
0.
0.
2.37
-0.33
=
1
kmln
=
1
kmax -
465
sum of diagonal elements of resolution matrix for
resolution for p velocity model
17..j.
1
465
elements
-
317.892
resolution for s velocity model
11>
6818
t9~5
6818
9V5N
9*0
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0
0.91
0.95
0.95
0.91
0.84
0.70
0.90
0.95
0.96
0.95
0.90
0.76
0.72
0.92
0.92
0.82
0.78
0.62
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0.79
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