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RESEARCH Delineating the Exmouth Mantle Plume

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RESEARCH Delineating the Exmouth Mantle Plume RESEARCH Delineating the Exmouth mantle plume (NW Australia) from denudation and magmatic addition estimates Max Rohrman* 202 GLENWOOD DRIVE, HOUSTON, TEXAS 77007, USA ABSTRACT Volcanic margins are a class of large igneous provinces (LIPs) characterized by rifting-derived basaltic magmatism. This is commonly attrib- uted to extension-related lithospheric thinning, generating decompression melting. Another mechanism influencing magmatism on volca- nic margins is mantle plume–induced lithospheric thinning. Unfortunately, it is difficult to differentiate between these mechanisms because they seem to take place almost contemporaneously. Whereas rifted volcanic margins produce linear denudation and magmatic addition patterns, mantle plumes or active upwellings would generate more subcircular domal patterns. Here, I use magmatic addition and denu- dation patterns to discriminate between these scenarios in a data set from the volcanic margin offshore NW Australia. Seismic and well data results suggest the presence of a domal component that is used to delineate the Late Jurassic Exmouth mantle plume. This upwelling was centered on a highly extended and subsided continental fragment bounded by the present-day subsea Sonne and Sonja Ridges and includes the Cuvier margin and Cape Range fracture zone. The region is characterized by ~2.6 km of denudation and ~500 m of tectonic uplift, with erosion products acting as source material for the Early Cretaceous Lower Barrow delta. Denudation analysis indicates that only ~40% of the seismically detected magmatic underplate is melt related, with the effective underplate ~4 km thick near the locus of uplift and decreasing in the outer regions. Tectonic subsidence analysis, seismic stratigraphy, and plate reconstruction suggest that the plume-induced domal uplift preceded magmatism and breakup. Plume activity was followed by a westward-propagating hotspot track, possibly terminating in Greater India (present Tibet). LITHOSPHERE; v. 7; no. 5; p. 589–600 | Published online 17 June 2015 doi:10.1130/L445.1 INTRODUCTION bilities (e.g., Moore et al., 1999; Ribe, 2004; plexes and flood basalt extrusions (Ridley and Agrusta et al., 2013; Brune et al., 2013). Richards, 2010). Volcanic margins are rifted margins char- One of the defining tests for the presence of Rifted margin uplift at magmatic rifts is acterized by massive igneous activity. These a mantle plume or active upwelling has been commonly characterized by linear uplift par- features have been commonly explained as a the evaluation of domal surface uplift predicted alleling the rifted margin (e.g., Menzies et result of extension and decompression melting by theoretical models (e.g., Farnetani and al., 2002), as a result of decompression melt- over a thermal mantle anomaly of 100–150 °C Richards, 1994). However, recently, it has been ing and subsequent magmatic addition at the (e.g., White and McKenzie, 1989; White et al., proposed that the uplift pattern might be more breakup margin. Furthermore, rift flank uplift 2008; Rooney et al., 2011), which is generally complex and show higher-frequency uplift su- is also influenced by the flexural rigidity or the explained as plume induced (e.g., Courtillot et perimposed on a lower-frequency pattern as a equivalent elastic thickness of the lithosphere. al., 1999; Montelli et al., 2004). Other explana- result of the stress state and lithospheric struc- Part of the flank uplift is transient, as a result tions include small-scale convection or state an ture (e.g., Burov and Cloetingh, 2009; Burov of the thermal anomaly or plume temporarily absence of significant thermal anomalies due and Gerya, 2014). Moreover, it has been sug- elevating the rift margin above sea level and to fertile mantle (e.g., Korenaga et al., 2002; gested that there might be no uplift at all for a allowing initial flood basalts to flow downhill, Anderson, 2005). Crucial factors in modern thermo-chemical plume (Sobolev et al., 2011). before subsiding and forming seaward-dipping popular volcanic rifting models are the pre- Nevertheless, domal uplift is still character- reflector series (e.g., White et al., 2008). These rift history and timing of the thermal anomaly istic of many large igneous provinces (LIPs), features are often difficult to unravel in outcrop (e.g., Bown and White, 1995; Armitage et al., as indicated by abundant geological and geo- studies where large flood basalt outpourings 2010). These models assume that lithospheric physical data (e.g., Saunders et al., 2007). Two have obscured earlier vertical motions and ero- thinning can only be achieved by extension. types of uplift are generated by a plume; the sion events. Alternatively, later erosion might Traditionally, actively upwelling mantle or first is transient uplift due to an upwelling ther- have stripped away any evidence of earlier up- plume material was thought to flatten below mal anomaly. The second is permanent uplift, lift phases. However, better horizontal and ver- stiff lithosphere (e.g., Farnetani and Richards, owing to plume-induced partial melting of the tical resolution can be obtained on magmatic 1994). However, recent studies suggest that lithosphere, generating a magmatic underplate rifted margins from offshore seismic profiles lithosphere can be eroded by plume-generated or high-velocity body at lower-crustal levels tied in with hydrocarbon exploration wells. convective currents or gravitational insta- (e.g., Tiley et al., 2004). Moreover, underplat- The NW Australian offshore area has long ing of high-density mantle melts can lead to been recognized as a volcanic margin (e.g., *Present address: Murphy Oil Corp, 9805 Katy Free- fractionation and shallower magmatic activity, White and McKenzie, 1989; Coffin and El- way #G200, Houston, Texas 77024, USA. evidenced by regional dolerite intrusion com- dholm, 1994) characterized by minor postrift LITHOSPHERE© 2015 Geological | Volume Society 7 of| AmericaNumber 5| |For www.gsapubs.org permission to copy, contact [email protected] 589 Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/7/5/589/3046387/589.pdf by guest on 24 September 2021 M. ROHRMAN subsidence and relatively limited magmatic activity (Symonds et al., 1998), with a large Seismic profile Gascoyne COT Abyssal intrusive component sourced by an underlying plain 1 N high-velocity body (Rohrman, 2013). Theories SDR Galah Gascoyne on the origin of the NW Australian LIP (Fig. 1) Lower Barrow delta Volcanic margin 18°S have been hampered by poorly constrained spa- gabbro Province Exmouth sill complex 3 tial and temporal evidence. Legacy models for plateau the LIP propose either a loosely constrained flood basalt 4 km A ESP and OBS profiles mantle plume without a clear hotspot track, or a J1 rifting-related mechanism (e.g., Mihut and Mül- selected wells B 2 ODP ler, 1998; Karner and Driscoll, 1999; Mutter et Pilbara craton E1 NG1 20°S 766 I1 al., 1989; Hopper et al., 1992). However, due to V1 bathymetry extensive seismic-reflection coverage and vari- 4 ous exploration wells drilled by the hydrocarbon S1 industry, this region provides an excellent natu- Sonja A1 ral laboratory in which to study the relationships Ju1 Ridge 5 Cuvier O1 22°S among magmatism, uplift, sedimentation, and Quokka YE1 breakup. In this article, I focus on: (1) estimat- Sonne margin Rise Cuvier Pa1 ing the spatial extent and relative amount of up- Ridge SP1 Abyssal H1 lift from observations on denudation (erosion), P1 magmatic addition, and sedimentation, and plain (2) explaining the results with a simple isostatic Wallaby mass balance and a one-dimensional melting Plateau Bernier model. The findings suggest the presence of a platform WS 100 km mantle plume before margin breakup in the NW 108°E 112°E 115°E Australian region. Moreover, the results explain most of the currently available data. Figure 1. Map of Exmouth region. SDR—seaward-dipping reflector series, COT— continent-ocean transition, BSB—Barrow subbasin, PS—Peedamullah Shelf, CRFZ—Cape Range fracture zone, WZFZ—Wallaby Zenith fracture zone. Vinck-1 GEOLOGIC SETTING (V1), Eendracht-1 (E1), Investigator-1 (I1), Sirius-1 (S1), Herdsman-1 (H1), Pendock-1 (P1), Sandy Point-1 (SP1), Paterson-1 (Pa1), Onslow-1 (O1), Jurabi-1 (Ju1), Jupiter-1 The NW Australian margin (Fig. 1) consists (J1), Yardie East-1 (YE1), Anchor-1 (A1), and North Gorgon-1 (NG1) are the main of a number of basins and continental fragments exploration wells used in this article. Deep seismic lines are from the literature with that formed as a response to several extensional observed high-velocity body (seismic velocities ≥ 7 km/s; numbered 1–5): 1—Fomin episodes (e.g., Longley et al., 2002; Gibbons et et al. (2000); 2—Mutter et al. (1989); 3—Goncharov et al. (2006); 4—Lorenzo et al. al., 2012). The south is characterized by Paleo- (1991); 5—Hopper et al. (1992). ODP—Ocean Drilling Program site; OBS—ocean bot- tom seismometer; ESP—expanded spread profile; WS—Wallaby Saddle. zoic basins such as the Bernier Platform. Further to the north, there are the Mesozoic Exmouth subbasin, Barrow subbasin, and Exmouth Pla- teau, while to the west, there is the fragmented and poorly known Wallaby Plateau (Fig. 1; Say- tectono- global ers et al., 2002; Stagg et al., 2004). Age (Ma) stage magmatics sea level lithology formation The main basin-forming event took place in Aptian rift NESB EP SESB the Late Permian to accommodate up to 7 km st 100m po Muderong Shale of deltaic Mungaroo Formation (Fig. 2). In the 125 Barremian -------------- p -------------- Hauterivian -------------- Exmouth subbasin and Barrow subbasin, Late ku ……………. Birdrong sandstone Valanginian t ………… Early underplating ………… Lower Barrow gp Triassic and Middle Jurassic extension provided Cretaceous Berriasian brea ………… accommodation for a thick Jurassic section Tithonian atic --….. Dupuy sandstone 150 e uplif (Fig. 2), while on the Exmouth Plateau, exten- Late Kimmeridgian gm 0m ----- Dingo claystone Oxfordian ---- plum ma ----- sion was limited, and the Early to mid-Jurassic Callovian Bathonian ------ Athol fm interval is a highly condensed section, bounded Mid Bajocian n ….
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