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Geophysical Evidence for a Deep Crustal Root Beneath the Yilgarn Craton and the Albany-Fraser Orogen

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Geophysical Evidence for a Deep Crustal Root Beneath the Yilgarn Craton and the Albany-Fraser Orogen Geophysical evidence for a deep crustal root beneath the Yilgarn Craton and the Albany-Fraser Orogen Hugh Tassell* Alexey Goncharov Geoscience Australia, Geoscience Australia, Australia Australia [email protected] [email protected] Line 19 of survey GA280, extending across the offshore Bremer Sub-basin, the Albany-Fraser Orogen and into the SUMMARY Yilgarn Craton. The resulting crustal model provides constraint to the crustal structure beneath the Albany-Fraser Using a marine seismic reflection survey as a source for Orogen and the southern margin of the Yilgarn Craton. onshore and offshore seismic refraction recorders, high quality refraction data were recorded to a maximum offset of 400 km. A two-dimensional velocity model for Line 19 of Geoscience Australia survey 280 in the Bremer Sub-basin and its onshore extension was derived by forward modelling using iterative ray tracing. Our velocity model indicates the presence of a deep crustal root located under the southern margin of the Yilgarn Craton and the Albany-Fraser Orogen. Comparison of the gravity response derived from this model with the gravity profile extracted from regional grids shows reasonable correlation. However, fine tuning of the seismic model is required to better define the complex geometry of the crustal root. Deep crustal roots are common under Proterozoic mobile belts that surround Archaean cratons. However, these results also indicate the presence of a crustal root under the southern margin of the Yilgarn Craton. This is consistent with the view that Proterozoic taphrogenesis penetrated tens of kilometres into the Yilgarn Craton. Key words: SW Australia, Bremer Sub-basin, Yilgarn Craton, Albany-Fraser Orogen, seismic refraction, gravity. Figure 1. Location of survey GA280 onshore land seismic stations (black dots) and seismic reflection lines (red). Background image is a high-pass filtered Bouguer gravity INTRODUCTION anomaly. As part of the Australian Government’s New Oil initiative, GEOLOGICAL SETTING Geoscience Australia undertook a geophysical survey (Southwest Frontiers, GA280) of the south-western Australian Exposed to the north of the Bremer Sub-basin are rocks of the continental margin in late 2004. The survey acquired 2700 km Palaeoproterozoic Albany-Fraser Orogen (Fig. 1), which of industry-standard, 106 nominal fold seismic data recorded extends along the southern margin of the Archaean Yilgarn to 12 seconds two-way time using a 6–8 km digital streamer Craton (Myers, 1990). Rocks of the Albany-Fraser Orogen and 4900 cui gun array. Marine seismic reflection acquisition comprise granitoid intrusions, orthogneisses, metagabbros, was supplemented by recording of refracted data from the mafic dykes and metasediments (Fitzsimons et al., 2003, same source by sonobuoys at sea and land recording stations Abeysinghe, et al., 2002 & Myers, 1995). These are basement (Fig. 1). The key scientific objectives of the refraction to the onshore Eocene sediments of the Bremer Sub-basin, component of this study were: which are extensively eroded, and fill the low-relief basement topography in discontinuous pockets close to the coast 1. Provide estimates of crustal thickness to better constrain (Hocking, 1990). The area has been subject to prolonged interpretation of tectonic evolution of the region, erosion and the subdued topography is extensively covered by 2. Provide accurate seismic velocity information to define the Cainozoic regolith (Abeysinghe, et al., 2002; Myers, 1990). nature of the basement and crust, and 3. Provide accurate seismic velocity information to improve The Albany-Fraser Orogen is thrust against and truncates depth conversion of reflection seismic data. granite-greenstones of the Yilgarn Craton to the northwest and extends eastwards under the Eucla Basin to the Coompana This paper discusses the crustal velocity structure derived Block and Gawler Craton (Fitzsimons, 2003 & Gee, 1979). from modelling and interpretation of the north-south oriented Rocks of the Albany-Fraser Orogen which formed between AESC2006, Melbourne, Australia. 1 Deep crustal structure of SW Australia Tassell & Goncharov 2200 and 1200 Ma were emplaced during the collision of the starting model offshore was the measured water depth and an Yilgarn Craton margin and east Antarctica between 1300 and estimate of basement depth from interpretation of depth 1100 Ma (Myers, 1993, 1995). The Recherche Granite converted reflection data. Forward modelling of the sediment dominates the eastern region of Albany-Fraser Orogen and upper basement velocity profile was based on sonobuoy (Fitzsimons & Buchan, 2005). Early stage deformation of the data (Goncharov et al., 2005). Modelling was an iterative granite was followed by deposition of the Mount Ragged process involving revised identification of refracted and metasedimentry group comprising quartzite with minor pelite, reflected phases and aiming to minimise the difference which are assumed to unconformably overly the Recherche between computed and observed travel times of these phases. Granite (Fitzsimons & Buchan, 2005). Low grade metasedimentary rocks of Stirling Range and Mount Barren Travel times of main phases were modelled for all nine land units outcrop in the western part of the Albany-Fraser Orogen refraction stations. The general pattern of seismic phases next to its northern border (Fitzsimons & Buchan, 2005). identified in the experimental data is well reproduced by the final model, as illustrated in Fig.2, where modelled phase PREVIOUS INVESTIGATIONS arrivals closely match phase arrivals observable in the field data. Travel time mismatches for individual phases in the final Crustal velocity profiles from previous land seismic refraction model (simplified version presented in Fig. 3) are generally surveys reported in Mathur (1974) ,marked as ‘PMA’ in Fig. within + 0.2 s although at some anomalous locations 1, Dentith et al. (2000), marked as ‘PDN’ in Fig. 1, and mismatches of up to 0.5 s were observed. Given the Drummond (1988) are consistent with the granitic and complexity of the final model, this represents a close fit gneissic granite composition of rocks outcropping onshore in between observed and calculated arrivals. the region. Both in the southern margin of the Yilgarn Craton, and the Albany-Fraser Orogen, velocities in the range 5.9-6.2 BASEMENT AND CRUSTAL STRUCTURE km/s dominate the upper crust and extend as deep as 15 km in onshore measurements. Velocities in the range 5.2-5.7 km/s On a crustal scale, our velocity model correlates well with dominate in the basement imaged by the offshore sonobuoy others in the region. Mathur’s (1974) crustal thickness of 34 refraction study in Talwani et al. (1979) (PTA measurements km near Albany at PMA05 location (see Fig. 1) is consistent in Fig. 1). with our results as is a sub-crustal velocity of 8.1 km/s. However, our results do not support a three layer crust with REFRACTION DATA AND VELOCITY MODEL velocities 6.1, 6.6 and 7.3 km/s proposed by Mathur (1974). The two layer model of Dentith et al. (2000) with an upper crustal velocity gradient from 5.95-6.31 km/s and a lower The density of observations in the onshore component of this crustal from 6.90-7.05 km/s is also consistent with our model investigation is a significant improvement over previous in terms of crustal velocity stratification, but our mid-crustal experiments. Land recorder stations were deployed at 25-50 boundary is up to 12 km deeper than the 18 km proposed in km intervals and shots fired every 37.5 metres in contrast to Dentith et al. (2000). This mismatch suggests that there may Dentith et al. (2000) with three shots for each of two ~400 km be a sharp SW-NE deepening of the mid-crustal refractor long orthogonal transects with 27 stations recording half of between the Dentith et al. (2000) PDN02-PDN05 line (Fig. 1) each transect simultaneously. However, our observation and our land refraction line. scheme is limited in that data were recorded in only one direction, and with no recording at near offsets (for the most A key feature of the velocity model is the presence of a deep remote inland station the nearest shot was fired at 295 km crustal root located ~100 km inland from the coast (Fig. 3). offset (see Fig. 1)). As a result, the velocity model of the The presence of this root is well constrained by first arrivals upper crust for inland stations is not well constrained. and some subsequent phases recorded at several stations. This However, there is good agreement between the main phases is illustrated in Fig. 4 which displays a common offset gather recorded by the station at near offsets and those from more for travel times recorded at three land refraction stations. distant stations. This suggests that no significant inland lateral variation in the upper crust has been missed due to these limitations. The quality of the data in terms of continuity of arrivals, clarity of phase changes in the first arrivals, and signal-to- noise ratio is very high (Fig. 2). Useful signal was recorded up to a maximum offset of 400 km for the station located 295 km inland from the coast. Three major phases were identified in the first arrivals: refractions in the basement and upper crust, refractions in the lower crust, and upper mantle refractions propagating at ~8 km/s (Fig. 2). This pattern is consistent from station to station. In addition, at some stations deep reflections were identified and were originally interpreted as Figure 4. Common offset gather of travel times recorded reflections from the Moho (PMP). However, subsequent by three of the nine land refraction stations indicating the modelling has shown that they most likely originate beneath need for a crustal root (centred around 200km in Fig.3) the Moho (Fig. 2). underlying the southern margin of the Yilgarn Craton and the Albany-Fraser Orogen. A two-dimensional velocity model for Line GA280-19 (lower panel in Fig.
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