The Australia-Laurentia connection in the Paleoproterozoic to Mesoproterozoic supercontinent Nuna is thought to have initiated by ca. 1.6 Ga when both continents were locked in a proto-SWEAT (southwestern U.S.–East Antarctic) configuration. However, the longevity of that configuration is poorly constrained. Here, we present a new high-quality paleomagnetic pole from the ca. 1.3 Ga Derim Derim sills of northern Australia that suggests Australia and Laurentia were in the same configuration at that time. This new paleopole also supports a connection between Australia and North China and, in conjunction with previously reported data from all continents, indicates that the breakup of Nuna largely occurred between ca. 1.3 and 1.2 Ga.

The hypothesized connection between western Laurentia (North America) and eastern proto-Australia (Australia-Antarctica shield, hereafter referred to as Australia), initially proposed for the latest Paleoproterozoic to Neoproterozoic, is one of the most intensively studied connections in the Proterozoic supercontinents Rodinia and Nuna (Dalziel, 1991; Moores, 1991; Idnurm and Giddings, 1995). In supercontinent Nuna (also known as Columbia), it is thought that Australia and Laurentia were connected throughout much of the Mesoproterozoic (Zhang et al., 2012; Pisarevsky et al., 2014a). However, critical uncertainties exist regarding the configuration and longevity due to a lack of high-quality paleomagnetic data and uncertain geological correlations (e.g., Morrissey et al., 2019).

Zhao et al. (2002) proposed that Nuna assembled between ca. 2.1 and 1.8 Ga during a period of global-scale orogenesis and broke up between ca. 1.6 and 1.2 Ga, placing Australia in a SWEAT (southwestern U.S.–East Antarctic) configuration (Moores, 1991) with respect to Laurentia. Based on paleomagnetic data, the original SWEAT fit was refined to a “proto-SWEAT” configuration for the 1.74–1.59 Ga interval, with Australia located further north in a Laurentian reference frame (Payne et al., 2009). Reinvestigation of the available paleomagnetic data for roughly the same time interval, including new data for ca. 1.8 Ga (Kirscher et al., 2019), suggests that the original proto-SWEAT connection is valid at ca. 1.8 Ga, but a reorganization between ca. 1.7 and 1.6 Ga would have led to a slightly modified (proto-SWEAT) configuration. Given the inherent paleomagnetic uncertainties, the reorganization between Australia and Laurentia in Nuna could reflect either (1) a connection between the continents at ca. 1.8 Ga, followed by dextral shearing or a divergence-convergence motion that led to separation and reassembly at ca. 1.6 Ga (Betts et al., 2016); or (2) that a small ocean existed between the continents at 1.8 Ga that closed by ca. 1.6 Ga (Betts et al., 2008; Pisarevsky et al., 2014a; Nordsvan et al., 2018; Kirscher et al., 2019). Nevertheless, this reorganization indicates that assembly of Nuna was a protracted process and took place until at least 1.6 Ga, which is supported by concurrent orogenesis in eastern Australian and western Laurentia (Pourteau et al., 2018).

Although the refined proto-SWEAT configuration between Australia and Laurentia is supported by ca. 1.58 Ga paleomagnetic data, the breakup age is poorly constrained (Evans and Mitchell, 2011; Meert and Santosh, 2017). The formation of ca. 1.5–1.2 Ga basins along the western margin of Laurentia has been used to argue that Australia rifted from Laurentia during this interval (Zhao et al., 2004). However, detrital zircon populations in many of the Laurentian sequences are thought to have been sourced from Australia (Link et al., 2007; Medig et al., 2014), suggesting that the basins were likely intracontinental (Davidson, 2008). Paleomagnetic data indicate that Australia and Laurentia were together at ca. 1.58 Ga (Betts et al., 2016) and that the breakup was achieved by ca. 1.2 Ga (Pisarevsky et al., 2014b). Here, we report a new high-quality paleomagnetic pole from the ca. 1.32 Ga Derim Derim sills of Australia and discuss the configuration and breakup of the Australia-Laurentia connection and the implications for the Nuna supercontinent.

The Derim Derim sills intrude the ca. 1.5–1.35 Ga Roper Group of the McArthur Basin in northern Australia (Fig. 1) and are gently folded with tilts of <5° (Abbott et al., 2001). Thermal modeling of Mesoproterozoic natural-gas occurrences reveals that the Roper Group probably never reached temperatures >∼300 °C (Hoffman, 2016). U-Pb geochronology for the Derim Derim sills yields ages of 1327.5 ± 0.6 Ma (isotope dilution–thermal ionization mass spectrometry [ID-TIMS] on baddeleyite; Bodorkos et al., 2020) and 1312.9 ± 0.7 Ma (ID-TIMS on baddeleyite; Yang et al., 2020), both coeval (within uncertainty) with the 1325 ± 36 Ma (2σ) Galiwinku dikes in northern Australia (Bodorkos et al., 2020). Aeromagnetic expression of the poorly exposed Galiwinku dikes reveals a radial pattern that projects to where the Derim Derim sills intrude the McArthur Basin, further indicating that both sets of intrusions are part of the same large igneous province (LIP) (Zhang et al., 2017).

We collected 170 oriented block samples from nine sites of the Derim Derim sills, where each site corresponds to one sill, in two outcrop areas (Fig. 1; Table S1 in the Supplemental Material1). One site of the Derim Derim sills was obtained from a subvertical drill core (Altree-2, drilled by Pacific Oil and Gas Pty Ltd.; 15°55′28.698′′S, 133°47′7.980′′E), where samples of the sedimentary rocks from the overlying Corcoran Formation were also collected for a baked-contact test (Table S4). One site of the Galiwinku dike was also obtained from outcrop. For all samples, measurements proceeded with anisotropy of magnetic susceptibility (AMS), followed by natural remanent magnetization, then demagnetization using thermal (80% of all specimens) or alternating-field (AF; 20% of all specimens) treatments. Standard paleomagnetic laboratory and analytical procedures were used (see the Supplemental Material). AMS lineations range between northwest and northeast and define an average flow direction consistent with the orientation of the coeval Galiwinku dikes, supporting the hypothesis of a plume center located north-northeast of Australia (Fig. 1).

Rock magnetic studies of the Derim Derim sill samples indicate magnetite and/or Ti-poor titanomagnetite as the main magnetic phase (Fig. 1; Fig. S3 in the Supplemental Material). Prominent single-domain and/or pseudo-single-domain signals in most of the samples indicate that the sills carry stable remanence. Baked and unbaked sediments in drill core show slightly different magnetic mineralogy (Fig. S5). The degree of AMS is generally low (<1.06; Table S2; Fig. S1), typical of mafic intrusions (Ferré, 2002), and indicates the absence of any significant deformation after the emplacement of the sills. The Galiwinku dike is characterized by a different magnetic mineralogy, showing a prominent low-temperature phase potentially related to maghemite (Fig. S3i) and much weaker magnetic signals (Figs. S2e and S2f).

Thermal and AF demagnetization of the Derim Derim sill samples yield well-defined and comparable directional behavior leading to high-stability characteristic remanent magnetization (ChRM) directions that are generally well clustered (Fig. 1; Figs. S2 and S4). The ChRM directions are of one polarity except one site yielding an antipodal direction. Due to the lack of chilled margin contacts in outcrop, a baked-contact test was carried out in a drill core where chilled margins are exceptionally preserved. The azimuth of the drill core is unknown, so the drill-core sites cannot be used in the mean direction calculation. Nonetheless, the drill core has an azimuthally consistent reference line, so all drill core samples can be oriented relative to each other, which is sufficient for conducting the test. Two sedimentary host-rock samples near the contact with the Derim Derim sill (3 and 8 cm above) yield similar directions to the sill (Fig. 1G) and also have similar inclinations to those obtained from Derim Derim outcrops, indicating that the sill sites within the drill core likely retain a primary magnetization direction. Another three samples from the sedimentary host rock of the same core but ∼30 m stratigraphically above the contact show a well-defined ChRM with a completely different direction from that of both the sill and the baked samples (Fig. 1G), constituting a positive baked contact test, i.e., the sill ChRM was acquired at the time of cooling.

Combining eight site-mean directions of Derim Derim sill outcrops yields a mean ChRM direction of declination 183.6°, inclination 46.2°, and α95 (95% confidence for spherical distribution) = 13.7° for the 1.32 Ga Derim Derim sills, with a corresponding pole position at 76.5°S, 120.2°E, and A95 = 15.0° (Table S3). The Galiwinku dike site-mean direction was not included due to its large confidence interval (Table S3) and rock magnetic and directional differences. The Derim Derim sills pole demonstrably represents a primary thermoremanent magnetization, and can thus be used for paleogeographic reconstructions. This interpretation is based on: (1) the paleomagnetic results from the drill core, which constitute a positive baked contact test; (2) rock magnetic studies of the drill core, which reveal the presence versus absence of pyrrhotite in the baked versus unbaked zones of the sedimentary host rock, which indicates metamorphic changes in the mineral composition of the host rock due to baking (Fig. S5); (3) starkly contrasting paleomagnetic directions of the Derim Derim sills compared to the next-younger unit with paleomagnetism, the ca. 500 Ma Antrim Plateau Volcanics (McElbinny and Luck, 1970); (4) geomagnetic secular variation, which can be assumed to be sufficiently averaged given the number of sampled cooling units and a reasonable estimate of paleosecular variation (S [angular dispersion of poles] value of 21.51; see the Supplemental Material) for the paleolatitude; and (5) the presence of antipodal site-mean directions that overlap within uncertainties after reversing the polarity of one site (see the Supplemental Material for details; Fig. S4).

The paleomagnetic inclination of the Derim Derim sills indicates that Australia was located at a paleolatitude of ∼30° at ca. 1.3 Ga. Comparing these new data with coeval poles from Laurentia (Murthy, 1978) using the modified Australia-Laurentia fit from 1.65 to 1.58 Ga (Euler rotation of Kirscher et al. [2019]; Fig. 2; Table S7) indicates the two continents were in a similar configuration at 1.3 Ga. We propose that the Derim Derim sills pole, showing that Australia and Laurentia were in the same proto-SWEAT fit at ca. 1.3 Ga as they were at ca. 1.6 Ga, strongly suggests that this configuration was maintained throughout that time interval. Although published 1.6–1.3 Ga paleomagnetic poles from Australia and Laurentia permit this proto-SWEAT configuration during this interval, comparative data are not always coeval, and some are of low quality and/or have significant age uncertainties (Table S5). This new pole, being coeval with poles in Laurentia and showing the same configuration at ca. 1.6–1.3 Ga, provides robust support for the proto-SWEAT interpretation at ca. 1.58 Ga and, by implication, the correlation of the ca. 1.6 Ga Racklan and Isan orogenies in northwestern Canada and northeastern Australia, respectively (Thorkelson et al., 2001; Nordsvan et al., 2018; Pourteau et al., 2018).

Collectively, these data suggest that following their amalgamation at ca. 1.6 Ga, Australia and Laurentia were contiguous in the same proto-SWEAT configuration for at least ∼300 m.y. This interpretation does not support the correlation of ca. 1.5–1.4 Ga A-type granites in northern South Australia and Mexico (Morrissey et al., 2019), but instead agrees with the interpretation of northern Australian (e.g., Mount Isa inlier)–derived detrital zircon in the ca. 1.5–1.4 Ga lower part of the Fifteenmile Group (PR1 unit; Yukon, Canada) of northwestern Laurentia (Medig et al., 2014). The divergence of ca. 1.2 Ga paleopoles from Australia and Laurentia indicate that the continents were separated by that time (Pisarevsky et al., 2014b), constraining the breakup age of the proto-SWEAT connection at ca. 1.3–1.2 Ga.

These new data also support the connection between northern Australia and the North China craton, as proposed based on the correlation of paleomagnetic poles (Zhang et al., 2012; Pisarevsky et al., 2014a), ca. 1.4 Ga oceanic euxinic events (Mitchell et al., 2020) and ca. 1.3 Ga LIPs (Zhang et al., 2017). Our proposed configuration of Australia and the North China craton (Fig. 3) is similar to that of Zhang et al. (2017) with the modification that the North China craton is rotated slightly clockwise relative to Australia. This modified configuration is more compatible with the paleomagnetic data from both continents (Fig. 2; Table S5), while inferring a plume center related to the Galiwinku-Datong dike swarm to the present-day north of Australia (Zhang et al., 2017) (Fig. 1). The exact amalgamation age between Australia and the North China craton is still unclear due to a lack of paleomagnetic data (particularly from the North China craton; Wang et al., 2019). Lithostratigraphic similarities between the McArthur Basin of Australia and Yanshan Basin of north China (Zhang et al., 2018; Collins et al., 2019; Wang et al., 2019) suggest that the two continents were neighbors from at least ca. 1.8 to 1.3 Ga, and detrital zircon in <1.2 Ga North China craton sedimentary rocks indicates they might have been together longer (Yang et al., 2019). However, in contrast, new ca. 1.2 Ga paleomagnetic data from North China indicate that Australia and the North China craton had started to break apart at this time (Ding et al., 2020).

The core of Nuna, traditionally including Laurentia, Baltica, and Siberia, is thought to have been assembled by ca. 1.78 Ga (Wu et al., 2005). Paleomagnetic poles from these three core continents support the configuration in Figure 3 from ca. 1.7 Ga, although other arrangements have been proposed (Pisarevsky et al., 2014a). If the final collision between Australia and Laurentia occurred at 1.6 Ga, then the previously formed core of Nuna might represent a precursor large building block of the Nuna supercontinent, just like Gondwana was to Pangea (Nance and Murphy, 2019).

Our new paleomagnetic pole shows that the ca. 1.6 Ga Nuna configuration of Australia and Laurentia (Pisarevsky et al., 2014a ; Kirscher et al., 2019) likely remained until ca. 1.3 Ga, implying that Australia was a stable part of the Nuna core. While the connection between Laurentia and Siberia might have persisted longer, paleomagnetic data suggest that significant core components of Nuna were disassembled from 1.3 to 1.2 Ga (Fig. 2C) (e.g., Cawood et al., 2010; Pisarevsky et al., 2014b; Ding et al., 2020). Therefore, the ∼300 m.y. duration of a stable Nuna core between 1.6 and 1.3 Ga, during which the supercontinent exhibited a slow counterclockwise tectonic rotation (Fig. 2), is strongly supported by paleomagnetic data from several continents and implies that Nuna was the longest lived among the three known supercontinents.

Funding was provided by an Australian Research Council Laureate Fellowship grant to Z.-X. Li, Curtin University (FL150100133); a Key Research Program of the Institute of Geology and Geophysics, Chinese Academy of Sciences, grant (IGGCAS-201905), and National Natural Science Foundation of China grants (41890833 and 41888101) to Mitchell; a Ministry of Science and High Education of the Russian Federation grant (075-15-2019-1883) to Pisarevsky; and Future Energy Systems (FES) funds at the University of Alberta, Canada, to L. Wu. Access to the cores was provided by the Northern Territory Geological Survey and the Darwin Core Library (Australia). This is a contribution to the International Geoscience Programme 648 and is contribution 1526 from the ARC Centre of Excellence for Core to Crust Fluid Systems ( We thank Dennis Brown for handling the manuscript and Alan Collins, Phil McCausland, and one anonymous reviewer for impartial and constructive reviews.

1Supplemental Material. Materials and methods, five supplemental figures, seven supplemental tables, and references providing further detail on paleomagnetic and rock-magnetic results, sampling descriptions, performed analysis, and reconstruction data. Please visit to access the supplemental material, and contact with any questions.
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