Australia: The Land Where Time Began |
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Bedout High (Bedout Rise, Bedout Structure) see
Marusek Hypothesis
Situated off the northwestern margin of the
Australian continent, the Bedout High has been suggested to be an impact
structure, and one that is being seen by some as a prime candidate for
an end of
Permian structure. Drill cores taken from the top of the
structure have found melt rocks and impact breccias, and there are data
from seismic and gravity studies, that are consistent with the presence
of a buried impact crater. Silica glass, SIO2,
that was almost pure, and plagioclases that were fractured and
shock-melted, and spherulitic glass, have been found in the breccia. The
presence of a melt sheet is indicated by the distribution over hundreds
of metres of drill core of glass and shocked minerals. The Bedout High
is suggested by the available gravity and seismic data to be the central
uplift of a crater of similar size to that of Chicxulub. An Ar/Ar age of
250.1 ± 4.5 Ma has been determined for plagioclases separated from the
Lagrange-1 exploration well. In Permian-Triassic boundary sediments
worldwide, the reported presence of impact debris can be accounted for
by the location, size and age of the Bedout Crater (Becker et al.,
Source 1).
There has been considerable debate concerning
catastrophic mass extinction at the close of the Permian. Evidence has
been presented by Becker et al.
(1-3) and others (4-10) that a major impact was associated with the
extinction event that killed off more than 90 % of marine taxa. Included
in this evidence are fullerenes with extraterrestrial helium and argon
(1,7), fragments of meteorite (8), Fe-Ni-Si “metamorphosed grains” of
probable meteoritic origin (5,8,9) Fe-Ni metals with impact spherules
(6,10) and shocked quartz (4).
When the Chicxulub Crater was discovered that
occurred at the Cretaceous-Tertiary (K-T) boundary at the time of the
mass extinction event acceptance of the idea that an impact accompanied
the extinction event increased dramatically (11,12). Becker’s team
searched for a crater at the boundary on the Permian-Triassic (P-T) in
parts of the Southern Hemisphere that had once been part of the
supercontinent of Gondwana, as the evidence of impact was found to be
most abundant in continents in this region, such as Australia and
Antarctica. Based on the study of a single seismic line (13,14),
Gorter suggested that the Bedout (“Bedoo”) High off the coast of
northwestern Australia might be the central uplift of a large crater
dating to the end of the Permian. In this paper Becker et
al. describe the Bedout
structure and present evidence from drill cores, as well as seismic and
gravity data, and Ar/Ar dating of plagioclases that Bedout is an impact
crater that is large, buried, and occurred at the end of the Permian,
that is possibly the source of the P-T ejecta deposits that are
distributed globally.
Geology of the Bedout
structure
The Bedout High is part of the Roebuck Basin which
forms the continental margin of the Australian continent. Included among
existing studies are 2 regional seismic surveys that were conducted by
the Australian Geological Survey (AGSO) and the japan National Oil
Company (JNOC) (15) and 2 exploratory wells that were drilled 9 km apart
on the top and the flank of the Bedout High (Bedout-1 and Lagrange-1)
that extend to depths of 3,250 m (9,986 ft) and 3,273 m (10,738 ft),
respectively. These wells were both drilled through about 3 km of marine
and fluvial sediments that consisted of carbonates and occasional
interbeddefd siltstones and mudstones, dating from the Tertiary to the
Cretaceous, with sandstones that were interbedded with claystones,
siltstones and coal, Tertiary to Triassic, after which a breccia was
encountered from the Late Permian (16). The Bedout High was crossed by 2
of the 14 AGSO regional seismic lines. Also, 4 wells penetrated Permian
strata offshore that aid in defining the Bedout structure and
stratigraphy. In the Lagrange-1 and the Bedout-1 cores and cuttings,
Fluviatile and marine Keraudren sediments dating to the Middle to Late
Triassic, were deposited directly on top of the breccia of Late Permian
age.
At the present the Bedout High rises to several
kilometres above the surrounding basement (17). It is also suggested by
deep crustal reflections and seismic refraction velocities that the
Bedout High is underpinned by elevated middle and lower crust. Core and
cuttings, that were catalogued as basalts and referred to as a “volcanic
breccia”, were both recovered from the top of the top of the High. This
regional “volcanism” that was associated with the rifting of the
Australian continental margin has been classified as the “Bedout
Movement” of P-T age (18,19). There is a regional angular unconformity
at the top of the High, which is consistent with uplift and erosion at
the end of the Permian, immediately after the formation of the Bedout
High and termination of the Bedout Movement (20). The rifting of the
continental “Sibumasu Sliver” off northwestern Gondwana was coincident
with the formation of the Bedout High (21). The post-impact tectonism,
uplift, faulting and erosion during the Triassic and Jurassic that
resulted overprinted regionally the Bedout structure and deformed the
original complex morphology of the crater.
The Bedout Breccia
Lagrange-1 and Bedout-1 exploration wells both ended
in what was inferred to be volcanic breccia. 52 m - 30 m of cuttings and
22 m of core – were recovered from the breccia unit in Bedout-1, and 391
m of cuttings were sampled from the breccia unit in Bedout-1, and 391 m
of cuttings were sampled from the breccia unit in the Lagrange-1 drill
hole. A series of centimetre-sized clasts are displayed by the Bedout
core, some of which had variable banding and others that are poorly
sorted, with chaotic dips of 30o to 50o in hand
specimens, over the entire length of the core (20).
Throughout the core most of the clasts are dark
green and massive, appearing glassy in hand specimens, though in thin
section many are seen to be partially altered to fine grained chlorite
or a mixture of fine grained plagioclase, carbonate, and iron oxides.
From the lowest section of the core, at 3,044 m (9,986 ft), Becker et
al. identified unaltered glass and relic igneous mineral grains.
Also, large, highly fractured plagioclase phenocrysts were present in a
section from higher in the core at 3,041 m (9,977 ft). Many small rock
and mineral clasts in predominantly glassy matrix that had been
partially altered to chlorite are present in the basal 8 m of the core.
Evidence of flow structures is shown in brownish glass, and calcite was
observed as veins and cavities in several thin sections. The mineral
clasts are comprised of mostly single and multiple aggregates of
plagioclase, and the clasts are of glassy fragments. In the lower 8 m of
the core the complex mixtures are of very different textures that are
similar to the cores from inside the Chicxulub crater (22-25).
Shocked minerals surrounded by a matrix consisting
almost entirely of glass, with the exception that it has been altered to
chlorite, are contained in the clasts from 3,344 m (9,986 ft). Included
in the samples are shock-melted plagioclase that has been completely or
partially converted to glass, spherulitic glass, and pure silica glass.
Diaplectic glass (maskelynite), that has a composition that is identical
to that of the surrounding plagioclase anorthosite (An50), is
enclosed in plagioclase. Becker et
al. also identified grains that are stoichiometrically ilmenite,
heterogeneous silica glass, albite, sanidine, and a carbonate (CaCO3)
clast that is partially melted with fragmented ooids (26,27). Sanidine,
which was identified optically and confirmed by microprobe analysis of a
10-μm grain, has 43 % albite in solid solution with no sign of
segregation (microperthite).
The Lagrange-1 cuttings consist of various types of
partially crystalline and partly glassy rock that has a mostly basaltic
composition. Some of the fragments are identical to those present in the
Bedout core. At 3,255 m (10,679 ft) one of these fragments shows
feldspar crystallites (laths) in “swallowtail” terminations, which
indicates rapid crystallisation from the glassy matrix. Heterogeneous
compositions are displayed by the feldspar laths, and they are mixtures
of either pure albite or K-feldspar in their glassy matrix, as seen in
the backscattered image of one of the grains. These textures, chemistry,
mineralogy, and mixture of different fragments were interpreted by
Backer et al. as indicating
that the basal 8 m of Bedout-1 is an impact melt breccia.
The plagioclase crystals that are completely or
partially melted and fractured and abundant glassy clasts are most
diagnostic. The coexistence of silica glass rich in titanium is in close
proximity (within 1 mm) to silica glass that is slightly aluminous but
poor in titanium requires silicate liquid immiscibility that has not
been seen in terrestrial magmatic environments.
Features that are attributable to a melt that is
generated by impact include carbonate lithic fragments that have been
partially melted and recrystallised and spherulitic glasses, which were
partially altered to chlorite, that has a different chemical composition
from the glassy matrix. Magnesian-ilmenite is found as microlites in the
matrix is also a mineral that is not commonly present in volcanic rocks.
According to Becker et al. the glassy rock clasts can be attributed to the melting of
target materials containing sediments rich in magnesium, such as
dolomites, and common Fe-Ti oxides, such as magnetite, titanite
“sphene,” and rutile, which are found in crustal environments. Overall,
the compositions of the minerals and glasses of the Bedout core are
consistent with a heterolithic impact breccia, or suevite, that is melt
rich, that is formed by the heterogeneous melt formation and subsequent
quenching and crystallisation that is triggered by impact. Such
compositions are not known and are not likely to exist in terrestrial
volcanic agglomerates, lava flows and intrusive pipes. Individually,
these minerals may occur only rarely in volcanic or plutonic rocks,
though never in association with each other.
Natural volcanic processes, in particular, generate
silicate melts up to, though not exceeding, about 78 %. When taken as a
whole these features are most consistent with melting that is generated
by impact. Volcanism that is not associated with rifting does not
produce melts (glasses), nor does any other endogenous magmatic process.
Overall, the textures of these heterolithic fragments, especially the
Bedout glasses, are similar to the features of the Sudbury Onaping
breccia and the melt breccia that is found in the Chicxulub crater.
Ar/Ar dating of the
Bedout core
40Ar/39Ar dating was undertaken by Becker
et al. of the feldspar
concentrates from the Bedout-1 core and Lagrange-1 impact breccia by
step-heating and single crystal fusion experiments. It is indicated by
40Ar/39Ar dates on 6 individual plagioclases from
3,041 m (9,977 ft) obtained from the Bedout-1 core that the ages are
much younger than the overlying Triassic sediments. Significant
alteration in plagioclase grains and possibly K addition are revealed by
petrographic and microprobe examination of the Bedout core from 3,044
(9,986 ft) and 3,041 m (9,977 ft.). Individual grains of feldspar
display Heterogeneous chemical compositions resulting from alteration or
disequilibrium in the sample cuttings. The glassy matrix at 3,044 m
(9,986 ft.) has potassium concentrations that are extremely low, <0.1 %,
and proved to be unsuitable for 40Ar/39Ar dating.
A plagioclase at 3,255 m (10,679 ft.) from the Lagrange-1 cuttings,
which displayed the least alteration or disequilibrium, has an 40Ag/39Ar
age of 250.2 Ma, that has a plateau portion between 8 and 90 % gas
release at 250.1 ± 1 , consistent with the previous K-Ar measurements on
the plagioclase separate from Lagrange-1 (253 ± 5 Ma). In the Yacatan-6
melt rocks from the Chicxulub crater similar problems in dating
plagioclase separates were encountered (23).
Geophysical Evidence
Becker et al.
reinterpreted some seismic lines that had been provided by AGSO (18)
that had originally been interpreted by Gorter (13,14) when it was
confirmed that the Bedout High consists of an impact breccia and melt
sheet. For line S120-01 the revised chronostratigraphy includes the
Lagrange -1 and Bedout-1 stratigraphic sections, which correlated with
adjacent onshore seismic sections and wells (31), and the Ar-Ar and K-Ar
dating on the melt breccia. The top of the Permian is conformable with
the Bedout High, while the sediments from the Triassic unconformably
onlap onto the structure. A broad uplifted core of basement 40-60 km in
diameter elevated to a minimum of 6 to 9 km is displayed by the revised
seismic section. Inferred only from the seismic character correlations
(16) the “pre-Permian” strata are not imaged well in the seismic data,
yet they appear to show uplift with the basement core. As the deeper
material has not yet been sampled and dated, these sequences could
alternatively all be crater fill impact debris from the end-Permian. A
slight uplift of Permian and earlier strata was also detected by Becker
et al. at a radius of about
100 km from the centre of the Bedout High, though it is not clear that
this is a concentric feature. A central uplift is revealed beneath the
Bedout High, with about 6-7 km of vertical structure relief on
midcrustal isovelocities, was derived from ocean bottom seismometer wide
angle reflection and refraction data that had been collected along the
S120-01 line (32). The data, though less well resolved, also suggest
possible variations in Moho depth beneath the Bedout High (33). However,
it is difficult to assess if this Moho topography , as in the case of
the Chicxulub crater, results from the dynamic effects of the crater-
(and Bedout High-) forming process extending down to the base of the
crust (33-35) or is the result of later rifting of the continental
margin.
In the Early to Middle Triassic the Bedout structure
was emergent and is probably deeply eroded. In the Canning Basin,
onshore much of the section dating to the Permian and Early Triassic is
missing: over 0.5 to 1.0 km of section overall, and on topographic highs
as much as 2 km (36). The depth of erosion at Bedout is known, though it
is probable that the unconformity at the top of the Permian represents a
section that is missing. The Lagrange-1 well passes through several
hundred metres of the impact melt breccia, though it is not certain how
much more of the High is actual impact melt breccia. It is shown by both
the isostatic residual gravity model for the Bedout structure and the
Bouguer gravity over Chicxulub that a semicircular gravity low
surrounding the expression for the central peak. The resolution of the
offshore gravity data is unfortunately not of sufficient quality to
obtain a vertical derivative image, which generally is used to highlight
the gradient that are more subtle, as well as assessing the
geomorphometric parameters, including size, of the Bedout structure. The
diameter of the outer edge of the gravity low is about 100 km, and is of
similar size to the Chicxulub gravity low that is better resolved.
Comparison of the Bedout
structure with other impact structures
As was noted first by Gorter (13,14), the
geophysical expression of the Bedout High shows similarities to the
central uplift in other large impact craters. A characteristic negative
gravity anomaly that surrounds a gravity high, is a feature that led to
the initial discovery of Chicxulub (12), is produced by fracturing and
brecciation that resulted from the impact of large meteorites with the
crust. At Bedout there is just such an anomaly, though it is obscured
somewhat by other features of the crust that are derived from younger
tectonic overprinting, dating the Triassic and Jurassic. In the centre
of large terrestrial craters the gravity high is due to the central
uplift elevating basement rocks that are denser. The gravity high is
associated with a structural high at Bedout. At Chicxulub the central
uplift is seismically poorly imaged, and consists mostly of about 6 to 7
km of uplift of midcrustal isovelocities, and has a diameter of about 40
km to 60 km (33). According to Becker et
al. these dimensions are well
within the Bedout High, which suggests that Bedout may be about the same
size as Chicxulub, about 200 m in diameter. The slight uplift that was
noted at a radius of about 100 km at Bedout may be a subtle expression
if the outer rim, though this is speculative. If the Bedout High is a
central uplift similar to the central uplift at Chicxulub, then at
Bedout the erosion could be extensive. As the top of the central uplift
at Chicxulub lies about 3.5 km below the floor of the crater then
erosion could be extensive at Bedout (37).
Across Bedout the seismic profile is similar to one
across the Mjølnir Crater in the Barents Sea (38), with the exception
that the central uplift of Mjølnir Crater is much smaller at 1.5-1.2 km
high and 8 km wide. The central uplift of the Mjølnir Crater extends
well above the pre-impact surface and appears to be the result of
differential subsidence in the annular trough that surrounds the peak
under the load of pre-impact sediments (39). At Bedout strata dating to
the Permian are overlain by about 3-5 km of sediment, therefore it is
possible that the relief of the Bedout High has been altered by
differential subsidence since its initial formation.
Evidence for an impact
in Gondwana at the P-T boundary
At Bedout High a large impact crater is consistent
with the global distribution of impact ejecta at the P-T boundary and
helps to explain apparent anomalies in the global patterns. Large impact
ejecta fragments (>200 μm) have to date been found only in the P-T
boundary sites that are relatively close to Bedout. Meteorite fragments
that were recovered from the P-T boundary at Graphite Peak in Antarctica
are in a size range from 50 to 400 μm. Becker et
al. found shocked quartz that
ranged in size from 150 to 550 μm at Frazer Park, which is adjacent to
the well-known site at Wybung Head in the Sydney Basin (4) and grains up
to 250 μm at Graphite Peak in Antarctica. At Frazer Park and Graphite
Peak the shocked quartz comprises about 1 % of the quartz fraction,
compared to about 50 % at many K-T boundary sites (40). It was suggested
(Retallack et al., 1998) that such a small amount of shocked quartz at the P-T
boundary may impact a minor impact, though Becker et
al. interpret the low percentage as a product of dilution by
reworking of the ejecta in an environment of continental deposition. In
the Sydney Basin and at Graphite Peak the P-T boundary layer is a
claystone breccia 10-20 cm thick that contains abundant rep-up clasts
from the underlying soil (4), whereas the distal K-T boundary deposits
that are rich in shocked quartz are composed mostly of ejecta and are
less than 1 cm thick (41).
The maximum grain sizes of the shocked quartz from
Frazer Park and Graphite Peak match well with the maximum sizes of the
shocked quartz at the K-T boundary and their distance from Chicxulub
when the maximum grain sizes of shocked quartz from Frazer Park and
Graphite peak are plotted with respect to the distance from Bedout. It
has been demonstrated by Pope (42) that the global distribution of
shocked quartz at the K-T boundary is explained best by dispersal by
winds in the stratosphere and the settling of the particles through the
atmosphere. Becker et al.
suggest that this type of mechanism is not efficient in latitudinal
transport of debris and, therefore, shocked quartz from the impact at
Bedout would be dispersed mostly over the Southern Hemisphere. This
would indicate that a large impact at Bedout is consistent with the size
of the shocked quartz that have been found in Australia and Antarctica
as well as possibly explaining why such grains are not found further to
the north.
Elsewhere, Meishan in China and Sasayama in Japan,
metal nuggets of Fe-Ni-Si, oxides, and spherules ⁓30 to 200 μm in size
are found at the P-T boundary (5,6,8,43). Spherules with refractory
grains (Mg-Ni-Fe oxides and Si-Ca-Al oxides) of similar size from the
K-T boundary have been attributed to formation in the vapour plume at
Chicxulub (44), and a similar vapour plume origin has been proposed for
the P-T spherules (5,8). These products of high energy vapour plume
condensates in China and Japan without shocked quartz is consistent with
an impact at Bedout. According to Becker et
al. the apparent absence of
P-T impact ejecta from sites far to the north of Gondwana, in the
Laurasia supercontinent, that is now North America, Europe and most of
Asia, may also be a consequence of an impact at Bedout in the far
Southern Hemisphere, though more work is required to verify this
hypothesis.
Discussion
Becker et al.
presented evidence, geochemical, geochronological, biological and
petrological, linking the Bedout structure to impact deposits to the
end-Permian around the world. The difficulties involved in interpreting
old impact structures that have subtle expressions and not retaining
pristine characteristics of younger craters that are well-preserved such
as Chicxulub, are emphasised in the recognition of an impact breccia in
the Bedout High. Only the upper portion drill cores that were available
were sampled (about 22 m of the intact core at Bedout-1and 391 m of
cuttings at Lagrange-1, of the impact melt breccia and it was found that
they contained impact melt breccia materials that were mostly highly
shocked. According to Becker et al.
the shock pressure that were indicated in the Bedout-1 core were
sufficient to produce maskelynite (28), pressures of 35-45 GPa, and
silica glass, >45-65 GPa. These pressures were too high to preserve
planar deformation features in quartz, <35 GPa, though high enough to
form stishovite, 15-40 GPa, and possibly hexagonal diamond, 70-140 GPa
(45). Therefore other samples from Bedout High may produce additional
evidence of shock, stishovite, coesite, and diamond, if it is assumed
that suitable target rocks were present. Analyses in the future
similarly may isolate pristine mineral grains that could be used for
radiometric dating and therefore constrain better the age of the
end-Permian and its association with the P-T boundary that has been
hypothesised. Additional geophysical data, and possibly coring, are
needed to better determine the size of the structure.
The evidence of yet another impact event (within the
age uncertainty) with severe flood basalt volcanism raises the question
of the relation of such catastrophes to each other as well as to mass
extinctions (46) [see Marusek Hypothesis] (MHM). According to Becker et
al. there has been increasing speculation that the impacts of large
bolides have been responsible for processes such as continental flood
basalt eruptions and mantle plumes (47,48). It is suggested by present
models that if a volcanic outburst may be induced if a bolide strikes a
pre-existing hotspot. The probability of such an event occurring is,
however, extremely remote (49,50). In the case of Chicxulub, and now the
Bedout High, the locations of the craters are opposite, instead of
exactly antipodal to, the location of the volcanic province, the Deccan
Traps in the case of Chicxulub and in the case of Bedout, the Siberian
Traps. Melosh has calculated the amount of kinetic energy needed to
create the volume of the Deccan Traps, about 500,000 km3,
requires about 5 x 1023 J, or twice the amount of kinetic
energy that was generated by the Chicxulub impactor, 10 km at 20 km/s.
Becker et al.
suggest that it seems clear that an impact may not be the direct cause
of the volume of flood basalts; it may still act as a “trigger” for the
event. Ar-Ar dating at both Siberia and Deccan has shown that volcanic
rocks that have mantle plume affinities predate the main pulse of the
Deccan and Siberian trap (51,52). Therefore the impact(s) and the sudden
release of energy might enhance the catastrophic eruption of a
pre-existing mantle plume. In order to properly assess, identify and
confirm extraterrestrial impact events and to understand further the
impact processes and their relation to severe volcanism and mass
extinction events in the geological record may require new models to be
considered.
Evidence has been presented by Becker et al.,
geochemical, biological and petrological, that genetically links the
Bedout Structure to the worldwide impact deposits of end-Permian age
(Fig.1, Source 1). According to Becker et
al. the Bedout High is an
example of old impact structures that have not retained the normal
characteristics of younger impact craters such as Chicxulub (Hildebrand
et al., 1991), the Bedout High being suggested to be a possible
impact structure by the recognition of impact breccia. Only the upper
portion of the Bedout High has been sampled, there ~22 m of intact drill
core from Bedout-1 and 391 m of cuttings from Lagrange-1of the impact
melt breccia, most of the material having been highly shocked. The shock
pressures of 35-45 GPa recorded in the core from Bedout were high enough
to produce maskelynite (French, 1998), and >45-65 GPa, to produce silica
glass. The pressures are too high to preserve PDFs in quartz (<35 GPa),
though high enough to form stishovite (15-40 GPa) and possibly hexagonal
diamond (70-140 GPa) (Stöffler, 1972).
Becker et al. suggest that the evidence from the
Bedout High adds to the growing evidence for a link between impacts and
flood basalt eruptions, based on the impact event being coincident,
within the age uncertainty, with severe flood basalt volcanism. They
also suggest that the question is raised of the relationship of such
catastrophes with each other, as well as with
mass extinction events (Richow et al., 2002). Speculation
has been increasing that the impacts of large bolides have been
responsible for processes such as eruptions of continental flood basalt
and mantle plumes (Jones et al., 2002; Glickson, 1999).
Present models suggest that volcanic eruptions may
be induced by a pre-existing hot spot being struck by a bolide,
though the probability of such an event is extremely remote (Melosh,
2000; Ivanov & Melosh, 2003). The craters at Chicxulub and Bedout, are
opposite, not exactly antipodal (Fig.1, Source 1) to the volcanic
provinces of Deccan and Siberia respectively. The amount of kinetic
energy required to create the volume of the Deccan Traps has been
calculated (Melosh, 2000), about 500,000 km3, about 5 x 1023
J, twice the amount of the kinetic energy generated by the Chicxulub
impactor (10 km at 20 km/s). Becker et
al. suggest the impact may not be the direct cause for the volume of
flood basalts; it may act as a trigger of the event. According to Becker
et al. volcanic rocks with
affinities to mantle plumes have been shown to predate the main pulse of
flood basalt at both the Deccan Traps and
Siberian Traps.
This suggests that the catastrophic eruption of a pre-existing mantle
plume might be enhanced by the impact(s).
Evidence of an impact dating to the
Permian-Triassic
boundary
is most abundant in the Southern Hemisphere, in the continents that were
part of
Gondwana, such as Australia and
Antarctica. This led Becker et al. to
concentrate their search for an impact crater in these continents.
Gorter suggested that the Bedout ("Bedoo") High might be the central
uplift of a large end-Permian impact crater, based on a single seismic
line (Gorter, 1996; Gorter, 1998). The Bedout High is in the Roebuck
Basin that forms the northwest margin of the Australia continent (Fig.2,
Source 1). A number of studies have been carried out on the Bedout High.
AGSO carried out 2 regional seismic surveys and the Japan Oil Company,
the quality of the data from the Japan Oil Company surveys being from
poor to moderate, the results were being reprocessed in an attempt to
improve quality. On the top and flank of the Bedout High 2 exploratory
wells, Bedout-1 and Lagrange 1, were drilled 9 km apart, extending to
3,052 m (9,986 ft) and 3,273 m (10,738 ft) respectively (Fig. 2 and fig.
S2, Source 1). Both wells reached a breccia dating to the Late
Permian (Smith, 1999, fig. S2),
after passing through about 3 km of marine and fluvial sediments,
comprising carbonates, with some interbedded siltstones and mudstones,
that have been dated to the Cretaceous to Tertiary, as well as
sandstones interbedded with claystones, siltstones and coal,
Triassic to
Cretaceous. The AGSO crossed the
Bedout High with 2 of their 14 seismic lines (Source 1, Fig. 2). There
were also 4 wells offshore helping to identify seismic reflectors
defining the structure and stratigraphy of the Bedout High, which
penetrated Permian strata, 2 of which are shown in Fig. 2 (Source 1).
Fluviatile and marine Keraudren sediments, from the Middle to Late
Triassic, in cores and cuttings from Lagrange-1 and Bedout-1, show
sediments that were deposited directly on top of the breccia from the
Late Permian (Source 1, Fig. 4, figs. S2 & S3).
The Bedout High reaches several kilometres above the
surrounding basement at present (Purcell & Purcell, 1994). The Bedout
High is suggested to be underpinned by elevated middle and lower crust
by deep crustal reflections and seismic refraction velocities. The core
and cuttings catalogued as basalts, which have been referred to as
"volcanic breccia", are from the top of the High. The "Bedout Movement"
from the P/Tr boundary, is the regional volcanism associated with
rifting of the Australian continental margin (Purcell & Purcell, Eds.,
1994). At the top of the High there is a regional angular unconformity,
which is consistent with uplift and erosion at the end-Permian, which is
immediately after the Bedout High formation and termination of the
Bedout Movement (Well reports Lagrange-1 & Bedout-1, 1971, 1983). The
continental "Sibumasu Sliver" rifted off northeastern
Gondwana, coincident with the
formation of the Bedout High (Charlton, 2001). The complex crater
morphology was deformed and the Bedout structure was overprinted by the
tectonism, uplift, faulting and erosion that occurred in the Triassic
and Jurassic as a result of the impact.
James Marusek
proposed a mechanism that could link very large impacts with the
Siberian Traps and Emeishan Traps, in China.
See Source 1 for more detailed information
1.
Becker, L., R. J.
Poreda, A. R. Basu, K. O. Pope, T. M. Harrison, C. Nicholson, and R.
Iasky. "Bedout: A Possible End-Permian Impact Crater Offshore of
Northwestern Australia." Science 304, no. 5676 (June 4, 2004 2004):
1469-76.
2.
Bedout: A Possible End-Permian Impact
Crater Offshore of Northwestern Australia |
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Author: M.H.Monroe Email: admin@austhrutime.com Sources & Further reading |