Download Seismic reflection profiling in the Proterozoic Arunta Block, central

Tectonophysics,
Elsevier
257
173 (1990) 257-268
Science Publishers
B.V.. Amsterdam
- Printed
in The Netherlands
Seismic reflection profiling in the Proterozoic Arunta Block,
central Australia: processing for testing models
of tectonic evolution
B .R . GOLEBY
‘3 *, B.L.N.
KENNETT
*, C. WRIGHT
r, R.D.
1 and K. LAMBECK
SHAW
*
’ Bureau of Mineral Resources, G. P.O. Box 378, Canberra, A. C. T. 2601 (Awtraha)
.’ Research School of Earth Sciences, Australian
National
(Received
September
Wright,
C., Shaw,
Uniuersity, G.P.O. Box 4, Canberra, A.C. T. 2601 (Austrd~a)
30, 1988; accepted
April 13, 1989)
Abstract
Goleby,
B.R., Kennett,
Proterozoic
Arunta
D.M. Finlayson,
Margins.
B.L.N..
Block, central
C. Wright,
Tectonophysics,
The region extending
change
in Bouguer
structures
geophysical
data
that would
result
thrusts
J.C. Dooley
from the northern
rocks
features
mapping
from “thick-skinned”
is evidence
address:
within
tectonic
with
Deformed
this region
A.C.T.
2601, Australia.
University,
(Editors),
of tectonic
Seismic
processes,
Probing
School
G.P.O.
of
in which
down
reflection
profiling
evolution.
In: J.H. Leven.
of Continents
.n the
anti their
Earth
Sciences,
is characterised
residuals,
Deep seismic
deformation
stacking
from surface
and
reflection
to the development
occurred
to at least the crust-mantle
the crust and displacing
Box 4, Canberra,
Province
travel-time
at the surface.
the help of unconventional
through
Arunta
have contributed
Zone that can be traced
of a fault extending
Research
National
K., 1990. Seismic
models
in teleseismic
are now exposed
Central Australia is characterized
by a series of
late Proterozoic-Palaeozoic
intracratonic
basins
(Amadeus
and Ngalia Basins) and exposed basement blocks of middle Proterozoic age (Musgrave
and Arunta
Blocks). Major east-west
trending
gravity anomalies
exceeding 1400 pm ss2 (Fig.
la), which are clearly related to the basin and
block structures,
also occur within the region.
Australian
Kennett
changes
Introduction
* Present
Lambeck,
for testing
Basin to the Northern
from the surface
have emerged
from the Redbank
The second
Amadeus
from the lower crust
and geological
of this model
and B.L.N.
Frn sm2 ), abrupt
(1400
or shear zones that extended
reflections
R.D. and
processing
173: 257-268.
gravity
in which
Australia:
thrust
data,
of a crustal
moderately
boundary.
techniques.
outcrop
along
by z large
large
other
model
d pping
Two important
The first is a series of
to depths
of more than 110 km.
the Moho.
Teleseismic travel-time
anomalies in excess of 1.5
s over distances of a few tens of kilometres have
also been observed
across the Arunta
Block
(Lambeck and Penney, 1984; Lambeck et al., 1988)
(Fig. la). Both the gravity anomaly and the teleseismic travel-time
anomalies
within the Arunta
Block relate to the location of the Redbank
Deformed Zone (RDZ, Fig. lb) (Shaw el al., 1984;
Stewart et al., 1984) one of a series of thrust zones
that have been mapped within the Arunta Block
(Fig. lc). The geological, structural
and geophysical data from this region are sufficiently
anomalous to have attracted
the attention
of several
workers over the last twenty years. To date, models for the type of deformation
for the region
include a crustal compressional model. “thinskinned” in style, with faults terminating on a
mid-crustal sole thrust (Teyssier, 1985), a mechanical folding and thrusting model (Lambeck, 1983),
and a “thick-skinned” faulted block model (Shaw,
1987; Lambeck et al., 1988).
This paper concentrates on the interpretation
of 130 km of deep seismic reflection data obtained
from north to south across the Proterozoic Anmta
Block (A-A’ of Fig. 1). (Details of the seismic
survey have been given by Goleby et al., 1986,
1988.) As part of this interpretation, unconventional methods of data processing and display
were used to discriminate between “ thick-skinned”
styles of deformation, and
and “thin-skinned”
have enabled the RDZ to be imaged to depths of
at least 35 km.
The Arunta Block is a region of exposed Proterozoic crust that has been interpreted as a major
ensialic mobile belt (Shaw et al., 1984; Stewart et
al., 1984). It has been divided into three tectonic
provinces (Northern, Central and Southern: Fig.
lb), each of which has undergone separate histories of deformation and metamorphism. In the
vicinity of the seismic line, the Southern Arunta
Province is an amphibolite facies terrane made up
of granitic gneiss, whereas the Central Arunta
Province to the north is a granulite facies terrane
composed of felsic and relatively minor mafic
granulite. The granulites of the Central Arunta
Province were metamorphosed at depths of around
25 km at about 1750-1800 Ma (Black et al., 1983).
These two provinces are separated by the RDZ
(Fig. 1, b and c), the major structural feature
within the Arunta Block. The RDZ occurs as a
7-10 km wide easterly
trending
zone of
anastomosing mylonites dipping northwards at
around 45”. This zone has been interpreted as a
major Proterozoic crustal suture zone that has
been reactivated during the Alice Springs Orogeny
between 300 and 400 Ma (Shaw, 1987). Some
thirteen kilometres to the south, and running subparallel to the RDZ, is the Ormiston Nappe and
Thrust Zone (ONTZ), another thrust zone that
appears to have dominated deformation during
the last stages of the Alice Springs Orogcny. Iht
Northern Arunta Province, separated lrom tht
Central Arunta Province by large granitoid intrusions and by moderate to steep faults, consists 01
low-grade metasediments
of amphibolite
and
greenschist facies. The Ngalia Basin (Wells and
Moss, 1983) lies within the Arunta Block (Fig. la).
and its northern margin is also fault-controlled; it
is not an important feature on the seismic reflection section because the ma~mum sedimentary
thickness along the profile A-A’ does not exceed 1
km.
Processing
techniques
crustal reflections
for enhancement
of deep
The use of explosives as the energy source and
the limited fold of recording proved highly successful in producing a strong high-frequency signal that stacked well. Indi~dual reflection segments, however, were often short (typically lo-30
traces or 400-1200 m) and show a patchy
coherency, both within a single-shot gather and
across several shots. This variation in reflection
character raised serious doubts as to the validity
of conventional stacking for the data (Goleby et
al., 1987). The fragmented nature of the reflections also makes effective migration difficult.
In order to develop a crustal structure for the
region, we had to be confident of the geological
significance of the events observed on the seismic
sections. We therefore investigated a number of
different stacking procedures to generate a working section with minimum processing artifacts,
and in a form suitable for migration.
All processing was done using pseudo true-amplitude techniques. Although the processed seismic
reflection section did not require major efforts to
enhance the deep signals, the various stacking
techniques applied did emphasise different attributes of the data, thus assisting inte~r~ta~on~
The deep seismic reflection data therefore enable
a well constrained crustal model to be developed
to depths of about 40 km.
The display techniques we have investigated
include a single-fold display, the standard CMP
stack, median stack, coherency stack, Nth root
stack, and an energy stack. Each stacking tech-
PROCESSING
FOR
TESTING
MODELS
OF TECTONIC
259
EVOLUTION
(4
r 400
lb)
.. .
_..‘..
AMADEUS
CentrelArunte
Prownce
/granulite faciesj
Northern Arunta Province
/greenschrsf fac;es/
I
~
CENTRALARUNTA
cl
Southern Arunta.Prownce
famphibobte
faoes)
4
PROVIN
x
x
I
A’
Fig. 1. Location
Australian
cross-section
diagram
showing
seismic traverse,
the principal
LI. Gravity
tectonic
and teleseismic
(A-A’, in c) are also shown. The travel-time
north and Fiji-Tonga
elements
of the central
travel-time
anomalies
profiles
Australian
from Lambeck
are for earthquakes
from the east. L2, L3 and L4 are the positions
of shorter
region (b) and the location
of the central
et al.. 1988 (a) and a schematic
from two different
seismic traverses
regions:
recorded
geological
Japan
during
from the
1985.
N
0068i
S,d Cl3
OOsiLl
UJWWN:
VI
X3WlS d W 3
e=JlAOJd WJnJV
3Skl3AVtll
01
8
PROCESSING
FOR
TESTING
MODELS
OF TECTONIC
nique
showed
tional
CMP stack, and, as a combined
package,
deep
some advantages
over the conven-
aided the interpretation
crust.
The effects
these techniques
261
EVOLUTION
processing
of data from the
on the data
are discussed
after
using
effects. The coherency stack for the Arunta Block
data showed a preferential
enhancement
of the
shallow-dipping
were
used
procedure;
surface
displays
to gauge
conditions
along
the
this display
penetration,
the
effect
highlights
and
the
and comparison
entire
section
of the
stacking
variations
degree
of
in the
energy
with the single-fold
display showed where the signal was degraded or
destroyed by the stacking process. In most cases
the cause for this could be established.
All stacking methods showed some improvement
in data
clarity.
CMP (common
mid-point)
occurs
significantly
resulting
There
the
very
reduction
in
was a decrease
in
from amplification
of residual
stack
if the reflecting
from the horizontal.
Median stack
The median
ducing
stack was very success ‘ul in pro-
a quality
section
highest
and
n lowest
integer)
are rejected,
stacked.
This approach
for display
samples
(Fig. 3). The n
(n
is a positive
and the remaining
was excellent
data
are
in removing
noisy portions
of trace, or a single trace inconsistent with the rest of the traces of the same CMP
gather. Although
the final fold may be dramatically reduced, the results were often found to be
well worth it. If taken to the extreme, only the
median value is retained, giving a single-fold dis-
The effectiveness of the CMP stack depends
having
approximately
flat-lying
reflectors,
smearing
noise.
over
a marked
static effects.
display
Single-fold
reflectors
and produced
the background
below.
continuity
Single-fold
to flat
steep events,
surfaces
In addition
on
as
depart
there
play that “simulates”
a stacked
section.
Nth root stack
The Nth root stack technique
(Muirhead,
1968;
is relatively
little improvement
in the signalto-noise ratio with a low fold of cover, and this
McFadden
et al., 1986) has the ability to enhance
the signal-to-noise
ratio in the stack. It is good in
method,
reducing random noise events and in suppressing
noise spikes. Fourth,
eighth and sixteenth
root
like the others discussed
here, is degraded
by near-surface
complexities.
Within the Arunta
Block, the dips are steep and the fold is relatively
low. Nevertheless,
steep dips, results
in spite of the predominance
of
obtained using CMP stacks are
good (Fig. 2). The CMP stack for the Arunta
Block shows an improvement
over any of the
single-fold displays, but there is a reduction in the
frequency bandwidth,
information.
with loss of high-frequency
stacks
were
tried.
Each
Nth
root
stack
of the
Arunta Block data showed a marked decrease in
the background
noise where the signal was low.
Where reflected energy was strong, no improvement in contrast between events and noise was
found. Improvements
in continuity
varied over the
section, ranging from a good improvement
in the
northern
decrease
portion at shallower depths,
in continuity
at the southern
tll a marked
end.
Coherency stack
Energy stack
This coherency stack weights each stacked trace
by a measure of the coherency
of each of the
traces within each CMP gather. This is a one-dimensional coherency, based solely on traces within
each CMP. The technique enhances small-amplitude coherent events over incoherent
noise. It is
very susceptible
to any misalignment
caused by
near-surface-related
effects or residual dip-related
The energy stack was developed
to take advantage of the high level of reflected signal and is
similar to “reflection
strength displays” (Taner et
al., 1979), but instead of modulating
the stack
with the envelope of the energy density. the energy
within a specified
time gate is displayed.
The
energy within a sliding gate is computed
for each
co
Q
ts*S)
3Wll
0
N
3-
*I
PROCESSING
FOR TESTING
MODELS
OF TECTONIC
263
EVOLUTION
m
.2
e
t
s
264
trace, then summed for each trace in the stack. By
varying the gate length to match particular frequencies, an estimate of the variation in frequency
content across the section could be obtained. The
central value of each gate is assigned the computed energy level for that gate. An example of an
energy stack is shown in Fig. 4. The energy stack
has a number of advantages, since it allows the
interpreter to look at packets of energy rather
than the normal display of signal ~plitudes,
and
is not affected by signal polarity. It also enables
an easier correlation of events, because they stand
out more clearly over the generally noisy background on the seismic sections.
Summary
of display procedures
No single stacking method is significantly better than the others. However, we found there were
many advantages in using several types of stack,
because each assisted in identifying different
events. The persistence of many reflections through
the various stacked sections provide confidence in
their validity. The improvement in coherency obtamed with some of the stacking techniques over
the original CMP stack allowed the successful
migration of the data. In particular, the energy
stack of the Arunta Block data (Fig. 4) ~~~t~
the coherent events and greatly improved continuity, especially for the northerly dipping sequence
of faults. Because of this improvement, these
“pseudo line-drawing” sections can be successfully migrated. The best migration results were
obtained after either median or energy stacking
and display processes. The results compared
favourably with the results from migration of
line-drawings, and were a great improvement over
the original migration of the CMP stacked data.
Deep seismic reflection results
A migrated line-drawing of the deep seismic
reflection section from the Arunta Block is shown
in Fig. 5. The migration was accomplished with a
velocity-depth function ranging from 5.5 km s- ’
at the surface to 6.2 km s-’ at the greatest depths.
We are confident that the line-drawing shown here
is a faithful representation of the seismic reflec-
tion data, because of the similar characteristic?
emphasised by the various stacks. Ihis deep
seismic section shows several unusual features
The first of these features is the exceptionally
high strength and depth of penetration of the
reflected deep seismic energy, particularly in the
Northern Arunta Province. This is seen in Fig. 4,
where the signal is still strong at reflection times
of 14 s, while frequencies up to 80 Hz at reflection
times of 5-6 s and to 60 Hz at 6-10 s reflection
time are common, particularly within the Northern Arunta Province. This high-frequency content
implies that the rocks at these depths (15-18 km)
have a very high Q (low attenuation) (Goleby et
al., 1987).
The second feature is the series of northerly
dipping reflections across the section. These reflections correspond to the surface outcrop of
either mapped faults or shear zones, or to the
positions of faults inferred from aerumagnetic
surveys (Mutton and Shaw, 1979). One group of
these dipping reflections corresponds to the RDZ,
and can be traced with confidence to depths of
about 30-35 km, and may extend to 50 km depth
(Fig. 3). Seismological expression of this fault
zone is further discussed by Cao et al. (1990).
There are several shallower dipping reflectors
within the Southern Arunta Province. The strongest of these corresponds to the ONTZ, although
possible interaction between this thrust and the
RDZ is not clear.
A third feature of the data is the marked difference in the character of the deep seismic reflections between the Southern Arunta Province and
the region to the north (Fig. 3). Beneath the
Southern Arunta Province, the reflectors down to
30 km are predominantly sub-horizontal, but beneath the Central and Northern Arunta Provinces
they generally dip northwards at around 30-35”.
The boundary between this change of dip of reflectors coincides with the position of the RDZ.
Tectonic implications
Figure 5
the seismic
Central and
acterized by
summarizes the principal features of
sections. The surface geology of the
Northern Arunta Provinces is chara series of moderately dipping faults
PROCESSING
FOR
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S~~~~~~N
MODELS
OF TECTONIC
CENTRALARUNTA
265
EVOLUTION
PROVINCE
PROVINCE. t
NORTHERN
Is!00 -t-
--*
-
ARUNTA
+-.
PROVlNCE---180
NGALIA BASIN
___
.’
I
.
.*
Fig. 5. Interpreted
This section
Ormiston
mantle
crustal
Nappe
material
and Thrust
upthrust
anomalies
or shear
structure
(B) of the Arunta
has a V : H ratio of 1 : 1 at a velocity
zones.
Zone. In this interpretation
with part
of the Central
and the teleseismic
The
Block superimposed
of 6 km s-l.
seismic
travel-time
sections
RDZ
on a depth-migrated
refers to the Redbank
there is a marked
line-drawing
Deformed
offset on the crust-mantle
Arunta
Province.
This high-density
region
residual
anomalies.
The uninterpreted
line diagram
show
that
these faults have an apparent dip of about 40°, are
traceable to depths of around 35 km (Fig. 5), and
appear to divide the crust of this region into a
series of “blocks”,
each with a similar seismic
character and bounded by the dipping faults. Synthetic seismograms
calculated
for three-dimen-
of the seismic
Zone
boundary
is part
cause
and
section.
~ON7’2 to the
of some 15 km, with
for both
is shown above
the gravity
i A).
sional models of a faulted crust have shown that
such faults can generate recoverable
reflected signals (Cao et al., 1990).
Sub-horizontal
reflections
within
the crustal
“blocks”
occur (Fig. 5) and are interpreted
as
compositional
changes that indicate
the present
attitude of the original crustal layering (Goleby et
Computed
Residual
S:;;i;;N
-CENTRAL
PROVINCE -I
. _
AiUNTA
L
.
PROVINCE
16000---t--
.
Profile +ISO ymS*
NORTHERN ARUNTA PROVINCE
+-,
NGALIA BASIN
0
.
L
SEISMIC
REFLECTION
Gravity
zotm -;
18Ol
P.3 ,
t
MODEL
Fig. 6. Observed and computedgravity profiles along LI (Fig. I). l&e computed profiile is based on the interpreted deep seismic
reflection model (A) for the Arunta B&k. Ia B, crosses represent the computed profile and closed circles represent the the residual
profile 4 150 pm s-*. Numbers superimposed on A are the assumed rock densities, in g cmd3, used in the gravity catc&tions.
al., 1989). Within some blocks these sub-horizontal events are truncated against dipping faults,
suggesting that the deformation of the crust occurred by movement aIong these faults, with
minimal rotation of the crustal blocks.
North of the IlIogwa Creek Schist 2one (Shaw
et al., 1984) (the eastern extension of the Palaeozoic continuation of the RDZ), erogenic highstrain zones older than 2600 Ma appear to be
flat-lying (Ding and James, 19g5). M~~b~s
and Black (1974) suggest that the RD2 may origi-
nally have been a thrust zone, dating from about
1600 Ma. However, Shaw (1987) has suggested a
separate evolution for the crustal blocks north and
south of the RDZ until 1450 Ma and possibly
until 1100 Ma, based on Rb/Sr and 40Ar/39Ar
isotopic data, bulk lithology, structural Mstory
and rnet~o~~c
grade. This suggests that the
RDZ may originally have been a suture (Shaw,
1987).
The crust-mantle bound&y beneath the Northem Arunta Province is interpreted to be. at the
PROCESSING
base
FOR
TESTING
of the zone
35-40
OF TECTONIC
of strong
km, whereas
Province
MODELS
reflections
beneath
at about
the Southern
Arunta
it is most likely at the base of the lowest
reflectors
seen
at about
50 km depth
There may be a local crust-mantle
of about
20 km thickness,
(Fig.
transition
extending
seismic
refraction
east-west
profile
CDP
Wright
results
that
along
crosses
zone
an
with the
orthogonal
the reflection
15300 of Fig. 5 (Goleby
et al., 1990). This implies
5).
from 30 km
to at least 50 km depth. This is consistent
near
267
EVOLUTION
line
et al., 1988;
an abnormally
rocks of the Ngalia
granulite
Basin to 2.95 g crn3
1983; Shaw, 1987). Even if these lateral
persisted
for
to depths
only
anomaly,
about
50%
of
the
account
observed
have a much
gravity
shorter
wave-
et al., 1989). This suggests a deeper
for the major
gravity
variations
of 10 km, they would
and would
length (Goleby
origin
for the
facies rocks north of the RDZ (Lambeck,
contribution
field over the southern
to the observed
part of the Arunta
Block. Figure
6 shows the observed
ity anomalies
and those calculated
Bouguer
grav-
from a density
thick crust beneath the Southern Arunta Province,
with significant
variation
in crustal thickness be-
model of the crust, which is displayed in the lower
half of Fig. 6, and which is consistent
with the
tween the Southern
vinces, which creates
“faulted
long-term
cussed
mechanical
by
Goleby
and Northern
Arunta
Proa problem in explaining
the
stability
et al.,
of the region
1989).
The
(dis-
Amadeus
Basin to the south has up to 14 km of sedimentary
rocks (Lindsay and Korsch, 1989) and the gravity,
teleseismic travel-time anomalies, and deep crustal
reflection data, do not indicate any discontinuity
in the crustal structure between the southern part
of the Arunta Block and the Amadeus Basin. A
current crustal thickness of about 50 km, inferred
from an east-west
refraction
profile across the
northern part of the Amadeus Basin (Wright et al.,
1990) implies that the sediments were deposited
on an approximately
normal thickness crust (30
km), consistent
with a predominantly
compressional origin for the basin, particularly
in the final
stages.
This
is also consistent
served gravity
with both
field and the teleseismic
the ob-
travel-time
anomalies
(Fig. la). The zone of seismic
parency
(between
25 and 30 km depth)
transbelow
CDP 16000-16500
(Figs. 3 and 4), just above the
RDZ, is interpreted
as a region of mantle material
(Goleby et al., 1989); this suggests that significant
thrusting
has occurred
on both the RDZ and
ONTZ, and that high-velocity
and high-density
mantle material has been emplaced relatively near
to the surface beneath
the Central Arunta Province, as has previously been inferred from other
geophysical
1988).
data (Lambeck,
1983; Lambeck
et al.,
Gravity modelling
Measured densities of near-surface
from 2.5 g cm-j
for the Palaeozoic
rocks vary
sedimentary
block”
portantly,
plitude
anomaly
model
of
the model clearly
Fig.
predicts
and the wavelength
(Goleby et al., 1989).
of
5.
Most
im-
both the amthe
observed
Conclusions
When unconventional
processing methods were
used to process deep seismic reflection
data recorded within the Arunta Block, the fine details of
the deep crust were clarified and then used to
confidently
infer the style of crustal deformation.
Our experience
with the seismic data from the
Arunta Block leads us to recommend
experimentation with processing techniques
for similar data
from other regions in order to obtain the best
results.
refraction
The combination
profiles,
of seismic
gravity
reflection
observations
and
and
surface geological mapping has enable:d the construction of a model of the crust for the Arunta
Block that is consistent
with a recent
tion of teleseismic travel-time
residuals
interpreta(Lambeck
et al., 1988). These combined
data sets suggest
that the crust of the Southern Arunta Province is
underthrust
beneath
the overriding
lower crust
and uppermost mantle of the Central Arunta Province. The model of the crust is also consistent
with new geological, structural,
metamorphic
and
radiometric
data (Shaw, 1987) which indicate a
complex uplift and deformation
history which occurred by movement on moderately dipping faults.
The RDZ is the main structural
boundary
within
the Arunta
Block, and its planar
geometry
to
depths of about 35 km, together with the likelihood that mantle material forms the hanging wall
26X
of
the
main
skinned”
region
thrust
model
(Shaw,
data (Shaw,
zone,
supports
for the tectonic
1987; Goleby
“thickof the
et al., 1989). Isotopic
1987) show that a substantial
this structure
and during
developed
or imbrication
of lower
part of
at a time leading
the Alice Springs
a stacking
exposure
a
evolution
Orogeny,
producing
of the crust
crustal
material
up to
and
north
the
of the
Goleby.
B.R., Wright,
Arunta
Block
Goleby,
K.,
skinned”
crustal
Lambeck,
K.,
the
Nth-root-stack
program.
Mr.
I.
Chertok
drafted the figures. Rb-Sr isotopic studies to be
reported elsewhere were carried out in conjunction
with
Dr.
K/Ar
L. Black
isotopic
(BMR),
studies
and
40Ar/39Ar
with assistance
and
from Dr. P.
Zeitler and Dr. I. McDougall (Australian
National
University).
We thank Dr. B. Drummond
for his
central
Australia.
phys.,
and Stewart,
A.J., 1983. Rb-Sr
events
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