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The Precambrian history of the Lhasa terrane, southern Tibet is intensely debated, which hinders global plate tectonic reconstructions throughout the Proterozoic. Previous research on Precambrian basement has suggested that the Lhasa terrane originated from India or Africa, although the paucity of exposed pre‐Neoproterozoic rocks in the North Lhasa terrane (NL) has led to significant uncertainty. We document newly identified Neoarchean granites and Mesoproterozoic Guomangtso Suite from the NL. These pre‐Neoproterozoic rocks reveal a 2.62 Ga anorogenic rifting event and a 1.30–1.10 Ga transition from subduction to back‐arc extension, related to the 2.7–2.6 Ga rifting of the Pilbara Craton and the Proterozoic assembly between the North and West Australian Cratons, respectively. However, these tectono‐magmatic events have no equivalents in the South Lhasa terrane (SL). These observations suggest that the NL originated from Western Australia, and the NL and SL may have distinct origins. Plain Language Summary Constraining the origin and evolution of continental fragments plays a crucial role in validating the patterns in the growth of successive supercontinents. However, tracking the evolving paleogeographic position of these fragments, especially for those of Precambrian age without paleolongitude constraints, has proven difficult. We redefine the pre‐Neoproterozoic evolution of the Lhasa terrane, southern Tibet based on newly discovered Neoarchean and Mesoproterozoic rocks, which contain missing information about the pre‐Neoproterozoic evolution of the North Lhasa terrane (NL). We reveal the Neoarchean–Mesoproterozoic evolution of the NL and its affinity with Western Australia, which is clearly distinct from the Indian affinities of the South Lhasa terrane (SL) from the Paleoproterozoic to Mesoproterozoic. These findings suggest that the Lhasa terrane did not originate as a unified entity from India during the pre‐Neoproterozoic, as previously thought, but rather that the NL originated from Western Australia, with the NL and SL having distinct origins. Our study therefore shows for the first time key evidence identifying the origin of the NL before the Neoproterozoic. Key Points Newly identified 2.62 Ga granites in the North Lhasa terrane show affinity with the Pilbara Craton, Western Australia The 1.30–1.10 Ga Guomangtso Suite identified in North Lhasa documents the Proterozoic assembly of North and West Australian Cratons The North Lhasa terrane was connected with Western Australia before separating during the Neoproterozoic

Although Earth has a convecting mantle, ancient mantle reservoirs that formed within the first 100 Ma of Earth’s history (Hadean Eon) appear to have been preserved through geologic time. Evidence for this is based on small anomalies of isotopes such as 182W, 142Nd, and 129Xe that are decay products of short-lived nuclide systems. Studies of such short-lived isotopes have typically focused on geological units with a limited age range and therefore only provide snapshots of regional mantle heterogeneities. Here we present a dataset for short-lived 182Hf–182W (half-life 9 Ma) in a comprehensive rock suite from the Pilbara Craton, Western Australia. The samples analyzed preserve a unique geological archive covering 800 Ma of Archean history. Pristine 182W signatures that directly reflect the W isotopic composition of parental sources are only preserved in unaltered mafic samples with near canonical W/Th (0.07 to 0.26). Early Paleoarchean, mafic igneous rocks from the East Pilbara Terrane display a uniform pristine μ182W excess of 12.6 ± 1.4 ppm. From ca. 3.3Ga onward, the pristine 182W signatures progressively vanish and are only preserved in younger rocks of the craton that tap stabilized ancient lithosphere. Given that the anomalous 182W signature must have formed by ca. 4.5 Ga, the mantle domain that was tapped by magmatism in the Pilbara Craton must have been convectively isolated for nearly 1.2 Ga. This finding puts lower bounds on timescale estimates for localized convective homogenization in early Earth’s interior and on the widespread emergence of plate tectonics that are both important input parameters in many physical models.

Here, we report the first occurrence of two (Ca-Y)-phosphate phases in apatite crystals from ancient rocks from both the Barberton greenstone belt and the Pilbara Craton. First, a cubic Ca3Y(PO4)3 phase was observed in a sample of silicified tuff from the Mendon Formation from the Barberton greenstone belt. A second phase, corresponding to a synthetic compound with the formula CaYP7O20, was observed in a sample of black banded chert from the Hooggenoeg Formation of the Onverwacht Group and in a sample of chert from the Strelley Pool Chert Formation (East Pilbara Terrane). Based on the presence of these phosphates and specific textures revealed by transmission electron microscopy, we argue for the importance of dissolution-reprecipitation processes in the formation of these phosphate phases. Temperature was likely not the primary parameter controlling the crystallization of the Ca3Y(PO4)3 and CaYP7O20 phases. Instead, the REE-F complexes in an H2O solution and the specific budget of REEs and Y in apatite were likely responsible for the nucleation and formation of the (Ca-Y)-phosphate phases in the Archean rocks of the Barberton greenstone belt and Pilbara Craton.

Bernard Kubler measured illite 'crystallinity', the half-height width or full width at half maximum (FWHM) of the X-ray diffraction line of illite/mica at 10 Å, directly on the diffraction traces; this procedure has since been followed by the vast majority of workers. However, some workers have recently measured the FWHM of the fitted Pearson VII function rather than on the diffraction traces. The FWHM of this function for low-angle phyllosilicate diffraction peaks (FWHM*PVII) is almost consistently 'broader' than those measured directly on the diffraction trace profiles (FWHMtrace) by up to 0.08°Δ2θ for the broader peaks. The Pearson VII function shows gentle curvature ('smoothing') at its tops and fast fading of the tails relative to virtually all 10 Å diffraction traces. The broad FWHM*PVII results from the consequent lowering/'under-fitting' of the peak tops and the upper tails and compensatory broadening/'over-fitting' of the intermediate peak flanks. FWHM*PVII 'contraction' with respect to FWHMtrace and enhancement of the peak maximum is found on traces of muscovite strips. The fitting reliabilities of the Cauchy function are almost invariably better than those of the Pearson VII function. Their FWHM*Cauchy values are narrower for both the illite/mica 10 Å and the chlorite 7 Å reflections; although they still differ somewhat from the FWHMtrace, they are much closer, usually within 0.02°Δ2θ. This markedly lesser broadening of FWHM* of the Cauchy of the Pearson VII function is the result of its stronger top curvature and notably faster tail fading (less 'smoothening'). For higher-angle mica peaks, the FWHM* values of the Pearson VII and Cauchy functions converge, usually differing only by 0.01-0.03°Δ2θ for the 5 Å peak, and even less for the 3.3 Å peak. It is therefore strongly recommended that FWHM values of the illite/mica 10 Å reflections be measured on the diffraction traces rather than on fitted functions. Where peak fitting is unavoidable (e.g. in order to separate the contributions of adjoining, partly resolved or unresolved reflections on broadened 10 Å reflections), Cauchy rather than Pearson VII functions should be used.

In the absence of vegetation, wind systems would have been very efficient in reworking terrestrial sediments. As a consequence, the Precambrian sedimentary succession should theoretically be replete with aeolian deposits; however, Precambrian aeolianites are rare. Aeolian reworking of Precambrian fluvial sediments has been described by a number of authors. Earlier researchers have reported aeolian reworking of fluvial quartz-rich sandstone unit of the Beasley River Quartzite Member of the Lower Wyloo Group (LWG). The Nummana Member is the topmost lithostratigraphic unit of the LWG. Earlier researchers interpreted the Nummana Member as a shallow marine deposit. In this note, published petrographical data from the Nummana Member are reviewed, and new field, as well as petrographical, evidence is reported. Earlier researchers did not adequately explain the origin of rounded to well-rounded grains in the Nummana sandstone. Rounded to well-rounded quartz grains, in combination with pinstripe lamination, adhesion features, and dunes with high-angle (up to 317) foresets, confirm the aeolian origin of the Nummana Member. The occurrence of subaerial basalts with continental tholeiite affinity (the Cheela Springs Basalt) on top of the Nummana Member is consistent with its nonmarine interpretation. The nearshore to terrestrial LWG succession, including the Nummana aeolianite, indicates regression and consequent emergence of the depositional surface and high continental freeboard during the early Paleoproterozoic in Western Australia.

Ambient inclusion trails (AIT) are enigmatic microtubular structures created by the migration of mineral crystals through a lithified substrate. The decomposition of organic material has been suggested as the driving force for the crystal migration, but has yet to be rigorously tested. AIT may hold potential as a biosignature for investigating early life on Earth if the associated organic material can be shown to be biological. This paper attempts to test the formation mechanism and biogenicity of AIT from the c. 3400 Ma Strelley Pool sandstone of Western Australia using NanoSIMS technology. In doing so, we demonstrate the unique ability of the NanoSIMS to combine sub-micron scale imaging with in situ chemical and isotopic data, thereby enhancing our ability to evaluate the biogenicity criteria for Archaean microstructures. Enrichments of a suite of major elements (C, N, P, S) and trace elements (Co, Fe, Ni, Zn), often associated with biological processes, are found within several AIT in this sandstone. C and N enrichments are most common along AIT margins, and correlate with depletions of Si, O, Ca and Mg, indicating that this material is indeed organic in nature. δ13C values of this carbonaceous material average -26 per mil. Petrographic observations show that some of the AIT occur in the centre of detrital sandstone grains where they were sealed from later fluid flow and therefore preserve primary Archaean (bio)geochemistry. In contrast, AIT found around the outer edges of sandstone grains may contain more recent organic material introduced by later fluid migration and are an unreliable biosignature. Using the petrographic and geochemical data a multi-stage model for AIT formation and subsequent diagenetic modification is proposed. The possible sources of the primary organic material are discussed and we conclude that the data are consistent with a biological origin for these AIT. An abiogenic origin is more difficult to sustain but cannot yet be completely excluded for AIT in general.

The 3.46 Ga Marble Bar Chert Member of the East Pilbara Craton, Western Australia, is one of the earliest and best-preserved sedimentary successions on Earth. Here, we interpret the finely laminated thin-bedded cherts, mixed conglomeratic beds, chert breccia beds and chert folded beds of the Marble Bar Chert Member as the product of low-density turbidity currents, high-density turbidity currents, mass transport complexes and slumps, respectively. Integrated into a channel-levee depositional model, the Marble Bar Chert Member constitutes the oldest documented deep-sea fan on Earth, with thin-bedded cherts, breccia beds and slumps composing the outer levee facies tracts, and scours and conglomeratic beds representing the channel systems.

Recent radiometric dating of carbonates and banded iron-formations on the Kaapvaal Craton, southern Africa, has suggested that late Archaean and Palaeoproterozoic carbonate sedimentation was diachronous across the craton. We present new SHRIMP U-Pb zircon ages of 2583±5 Ma and 2588±7 Ma for two samples of a tuff bed, 320 km apart in the upper Oak Tree Formation, Transvaal Supergroup. These ages, in conjunction with published data, support previously established sequence stratigraphic correlations that show the temporal equivalence of late Archaean carbonates in the region. A review of the sequence stratigraphy and geochronology of the Mount Bruce Megasequence Set on the Pilbara Craton, Western Australia, and the newly named Highveld Megasequence Set on the Kaapvaal Craton, indicates a remarkably similar geohistory. Both cratons are characterized by a divergent megacycle (Hamersley Range and Vaal Megasequences) followed by a convergent megacycle (Chichester Range and Drakensberg Megasequences). Our data show that the megasequence boundary is marked by drowning of both cratons at approximately the same time (c. 2590 Ma), which permits more meaningful geotectonic correlations between them.

Compositional evolution of the Archean mafic-ultramafic volcanics is considered in comparison with evolution of the Paleoproterozoic volcanism using available data on the Baltic shield, Pilbara (Australia) and Superior (Canada) cratons, and the Isua greenstone belt (Greenland). The Archean volcanics of mantle origin are of two major types, represented (a) by komatiite-basaltic complexes (komatiites, komatiitic and tholeiitic basalts) and (b) by geochemical analogs of boninites (GAB) and siliceous high-Mg series (SHMS) of volcanic rocks. As is established, the komatiitic and GAB volcanism ceased in the terminal Archean, whereas the SHMS rocks prevailed in the Paleoproterozoic to become extinct about 2 Ga ago in connection with transition to the Phanerozoic type of tectonomagmatic activity. Geochemical trends of mafic-ultramafic associations occurring in the considered cratons are not uniform, being of particular character to certain extent. With transition from the Paleo- to Neoarchean, rock associations of both types reveal a minor increase in Ti and Fe contents. Comparatively high Fe 2 O 3tot TiO 2 , and P 2 O 5 concentrations (maximal ones in the Archean), which are characteristic of the Neoarchean (2.75–2.70 Ga) basalts from the Superior and Pilbara cratons or the Baltic shield, represent a result of relatively high-Ti intracratonic magmatic activity that commenced in that period practically for the first time in the Earth history. This magmatic activity of the Neoarchean was not as intense as the high-Mg basaltic volcanism, and the absolute maximum in concentrations of the above components was attained only 2.2–1.9 Ga ago, at the time of appearance in abundance of Fe-Ti picrites and basalts typical of the Phanerozoic intraplate magmatism. The Archean volcanic complexes demonstrate gradual secular increase in concentrations of incompatible elements (LREE inclusive) and growth of Nb/Th ratio that apparently reflected the progressing influence of mantle plumes. In the early Paleoproterozoic (2.5–2.35 Ga), values of that ratio considerably declined in the SHMS rocks and then quickly grew in the Middle Paleoproterozoic volcanics (2.2–1.9 Ga) to attain finally the values typical of the Phanerozoic magmas associated in origin with mantle plumes. The ɛ Nd (T) parameter was decreasing with time from positive values in the Paleoarchean to negative ones in the SHMS rocks of the Paleoproterozoic most likely in response to grown proportion of ancient crustal material in magmatic melts. Since the mid-Paleoproterozoic, the ɛ Nd (T) values turn in general into positive again reflecting change in the character of magmatic activity: the SHMS melts gave place at that time to the Fe-Ti picrite-basaltic magmas. The primary crust of the Earth was presumably of sialic composition and originated during solidification from the bottom upward of the global magma ocean a few hundreds kilometers deep, when most fusible components migrated up to the surface to form there the granitic crust. Geological history of the Earth commenced at the appearance time of granite-greenstone terranes and granulite belts separating them, the first large tectonic structures formed under influence of raising mantle superplumes.

Aim: We review the biogeography of the Pilbara, synthesize information on the geological and landscape history of this region and surrounds, and assess fine-scale genetic structure across multiple taxa to examine hypotheses concerning the distribution of genetic lineages. We use this to provide a baseline for future biological studies in an ancient area of endemism. Location: The Pilbara region, Western Australia. Methods: Literature is summarized, including the history of Pilbara landscapes and climate, and previous biogeographical work. We used mitochondrial DNA phylogenetic datasets of seven co-distributed gecko (diplodactyline and gekkonine) lineages to assess the monophyly of Pilbara lineages, and concordance with geological and habitat divisions. Results: The Pilbara harbours taxa genetically distinct from their non-Pilbara relatives, despite close geographical proximity of populations. This is emphasized at the eastern and southern margins of the Pilbara, where habitat gradients are pronounced. In contrast, the northern margin, where sandy substrates of the Pilbara meet the dunes of the northern deserts, exhibits little genetic differentiation. Within the Pilbara, diversification patterns are idiosyncratic and may reflect species-specific ecological differences. However, a repeated north/south partitioning of genetic diversity is evident across taxa. An additional emerging pattern is an east/west genetic division in the northern Pilbara, which may relate to major drainage divides and geological discontinuities associated with east and west Pilbara terrains. Main conclusions: The Pilbara is an area of exceptionally high biotic diversity and endemism. The broader biogeographical patterns revealed in our molecular analyses are consistent with those recently identified using species richness patterns of invertebrates. Future studies of additional taxa using multiple molecular markers will provide the means to test and refine the biogeographical hypotheses presented here. Understanding the biogeography of the Pilbara and the partitioning of genetic diversity across the ancient and heterogeneous landscape is of paramount importance in the face of rapidly expanding economic and developmental pressures.