Nanospheres of lead (Pb) have recently been identified in zircon (ZrSiO4) with the potential to compromise the veracity of U-Pb age determinations. The key assumption that the determined age is robust against the effects of Pb mobility, as long as Pb is not lost from the zircon during subsequent geological events, is now in question. To determine the effect of nanosphere formation on age determination, and whether analysis of nanospheres can yield additional information about the timing of both zircon growth and nanosphere formation, zircons from the Napier Complex in Enderby Land, East Antarctica, were investigated by high-spatial resolution NanoSIMS (Secondary Ion Mass Spectrometry) mapping. Conventional SIMS analyses with >µm resolution potentially mixes Pb from multiple nanospheres with the zircon host, yielding variable average values and therefore unreliable ages. NanoSIMS analyses were obtained of 207Pb/206Pb in nanospheres a few nanometres in diameter that were resolved from 207Pb/206Pb measurements in the zircon host. We demonstrate that analysis for 207Pb/206Pb in multiple individual Pb nanospheres, along with separate analysis of 207Pb/206Pb in the zircon host, can not only accurately yield the age of zircon crystallization, but also the time of nanosphere formation resulting from Pb mobilization during metamorphism. Model ages for both events can be derived that are correlated due to the limited range of possible solutions that can be satisfied by the measured 207Pb/206Pb ratios of nanospheres and zircon host. For the Napier Complex zircons, this yields a model age of ca 3110 Ma for zircon formation and a late Archean model age of 2610 Ma for the metamorphism that produced the nanospheres. The Nanosphere Model Age (NMA) method constrains both the crystallization age and age of the metamorphism to ~±135 Ma, a significant improvement on errors derived from counting statistics.
Geochronology is crucial to the understanding of geological processes, and SIMS (Secondary Ion Mass Spectrometry) U-Pb geochronology of zircon (ZrSiO4) has become the most widely used method for dating rocks that have undergone complex or multiple thermal events. Zircon contains trace amounts of three Pb-producing radionuclides: 238U → 206Pb, 235U → 207Pb and 232Th → 208Pb. Because 238U and 235U have half-lives of 4468 Ma and 704 Ma, respectively, 238U/206Pb and 235U/207Pb give independent age estimates. Concordance between these ages (and with 207Pb/206Pb) provides evidence that the U-Pb decay system has not been disturbed. However, U-Pb systematics of many zircons are disturbed, due to Pb mobility during geological processes such as metamorphism, fluid infiltration and weathering1,2,3,4,5,6,7.
The mechanism for such disturbance is initiated by radiation damage of zircon resulting from radioactive decay of U and Th, creating locally amorphous domains that contain the stable daughter isotopes of Pb8,9. With sufficient time and actinide concentration, the zircon becomes metamict, where amorphous domains overlap to form a continuous Pb-bearing network of damaged zircon between islands of crystalline zircon. A transmission electron microscope (TEM) study of zircons from the granulite-facies Napier Complex in Enderby Land, east Antarctica10, showed that Pb mobilization occurred during metamorphism, forming crystalline native Pb nanospheres typically <10 nm in diameter and 100s of nanometers apart. The authors interpreted this phenomenon as resulting from Ostwald ripening of radiogenic Pb accumulations during thermal annealing of metamict zircon. The formation of metal Pb nanospheres therefore effectively isolated them from further ingrowth of radiogenic Pb and from subsequent Pb loss. After metamorphism, continued U and Th decay resulted in the renewed accumulation of radiogenic Pb in the zircon between the Pb nanospheres. The migration of radiogenic Pb in zircon during metamorphism has been established by several techniques, including SIMS6,11,12,13,14,15, TEM10,16,17 and atom-probe tomography (APT)18,19,20,21.
Conventional SIMS analyses at 10 μm lateral resolution sample variable mixtures of Pb from nanospheres and from the zircon host, potentially giving unreliable ages. For example, Kusiak et al.11 demonstrated that 207Pb/206Pb ratio measurements of ~10 µm spots of concentrated radiogenic Pb yielded apparent ages ranging between 4.15 and 2.76 Ga from measurement sites only tens of micrometers apart in a zircon whose 207Pb/206Pb crystallization age was determined as 3.38 Ga by SIMS. This analysis scale is however still ~103 larger than typical nanospheres. In an alternative approach, Valley et al.18,19 and Peterman et al.20 used APT to analyze 207Pb/206Pb from a small number of Pb clusters (~103 Pb atoms) trapped in volumes of zircon ~103 nm3 and were able to show that 207Pb/206Pb ages could be deconvoluted using a Tera-Wasserburg plot to yield the zircon crystallization age and the Pb mobilization age. These authors concluded that the formation of Pb clusters had no influence on the U-Pb age. However, the situation is different in zircon from the Napier Complex in Antarctica, where areas containing metal Pb nanospheres, when analyzed by SIMS, gave variable ages without geological meaning. To solve this problem, we utilized NanoSIMS and hereby demonstrate that high spatial resolution mapping of large areas of zircon >100 µm2, with sufficient spatial resolution to analyze many individual nanospheres within that area, can directly yield both the zircon formation age and the timing of metamorphism that caused the Pb mobilization.
Theory and constraints on Nanosphere Model Ages (TNMA)
Measurement of 207Pb/206Pb allows a determination of age that is not subject to the uncertainties associated with U-Pb isotope calibrations if it can be assessed that there was no initial Pb in the zircon22. Nevertheless, the relationship between 207Pb/206Pb and its calculated age depends on maintaining the association between daughter and parent isotopes to the present day. If radiogenic Pb was dissociated from its uranium parent in the past, then its 207Pb/206Pb composition will not correspond to a 207Pb/206Pb ‘age’ as conventionally calculated.
The 207Pb/206Pb composition in this case may be derived if we assume that the zircon is formed at time T1 and with no inherited Pb. Uranium and Th decay in the zircon produce domains of radiation damage in the zircon lattice. At time T2, an event occurred which mobilized the Pb accumulated from U and Th decay within the zircon between T1 and T2. Such Pb mobilization most likely occurred during high-temperature metamorphism of the rocks in which the zircon resides, but can occur through other processes too, such as fluid-assisted coupled dissolution-reprecipitation, although the latter is more likely to remove radiogenic Pb and/or contaminate the zircon with Pb from outside the grains23. Mobilization causes Pb to aggregate into nanospheres as the Pb-incompatible crystal lattice of the zircon host is repaired. If there are no further Pb mobilization events and with no U or Th in the nanospheres, the 207Pb/206Pb composition of the nanospheres remains constant after T2. The Pb isotopic composition of the nanosphere formed at time T2 is therefore ‘frozen’ and the nanosphere represents an isotopic ‘fossil’ of its time of formation. Subsequent U and Th decay in the zircon host around the nanospheres between T2 and today produces further radiogenic Pb, and if the U and Th distribution is homogeneous then nanoscale observation reveals Pb nanospheres surrounded by radiation damaged zircon with a homogeneous distribution of radiogenic Pb.
The system may be understood using the Holmes-Houterman model22 in which the zircon formed at time T1 and the Pb was mobilized at time T2, with the 207Pb/206Pb ratio in the zircon at the time of Pb mobilization given by:
which will be the 207Pb/206Pb ratio retained within the nanospheres to the present day. The ratio 1/137.82 relates to the present day 235U/238U ratio, and λ235 and λ238 represent the decay constants for 235U and 238U, respectively. Subsequent U decay within the zircon host will produce a 207Pb/206Pb ratio representing radiogenic Pb accumulation until the present day22.
In this general model, the isotopic composition of radiogenic Pb that has accumulated from time T1 until T2 when the nanospheres form, and the evolution of the composition of radiogenic Pb in the zircon host due to subsequent actinide decay from T2 until the present day, is portrayed graphically in Fig. 1. A consequence of this model is that the 207Pb/206Pb ratio frozen into the nanospheres will be in the range of 2.007 > 207Pb/206Pb > 0.0464 for 4.54 Ga > T1 > T2 > 0, whereas the Pb within the host zircon formed after the Pb mobilization event will range from 0.618 > 207Pb/206Pb > 0.0464. The time T2 can be determined from the Pb isotopic composition of zircon in between nanospheres and if T2 may be determined, then T1 may be calculated from the Pb isotopic composition of the nanospheres.
In general however, with error limits on measured 207Pb/206Pb values for the nanospheres and zircon host, there is a limited, correlated range of possible values for T1 and T2 which can satisfy Eqs. 1 and 2. We term the model age solutions of this method the Nanosphere Model Age (TNMA).
There is an additional constraint that may be placed on T1 and T2: the quantity of Pb available for formation of the nanospheres is sensitive to the time difference (T1 − T2) and hence the proportion of nanosphere-hosted Pb relative to Pb in the zircon host provides an additional constraint on possible model solutions to T1 and T2 from the experimental data. Although T2 is primarily constrained by the 207Pb/206Pb composition in the zircon host, the uncertainty on this measurement yields a range of possible T1 values from Eq. (1). However, not all of these possible T1 values predict nanosphere 207Pb/206Pb values which fall within the range of experimental measurements. In other words, the constraint placed by (T1 − T2) on possible values for the 207Pb/206Pb in the nanospheres places additional constraints on the model age for T2. Model ages for the crystallization age and metamorphism are correlated and precision is better on the determined model T1 and T2 ages are better than the individual measurements of 207Pb/206Pb of nanospheres and zircon outside of nanospheres might imply. This is illustrated in Fig. 1 of the supplementary information.
The key assumptions in this method are that (1) all of the radiogenic Pb within the zircon at T2 is moved into nanospheres during the Pb mobilization event, so that no Pb remains outside of nanospheres dispersed in the zircon at T2; and (2) that there is no loss of Pb from the zircon to the host rock during the Pb mobilization event. If assumption (1) is invalid, the Pb isotope composition of nanospheres will remain as determined by Eq. (1) but the 207Pb/206Pb of the zircon host will be higher than predicted by T2 alone. If assumption (2) is invalid then the 207Pb/206Pb ratios of nanospheres will remain as predicted by Eq. (1), and the model ages T1 and T2 would be unaffected, but the amount of Pb in nanospheres compared to the amount in the zircon host measured today would be affected.
A significant consequence of the model is that for all values of T1 and T2 during Earth history (where T1 > T2 > 0) the 207Pb/206Pb ratio of the nanospheres and of radiogenic Pb in the host zircon, as measured today, would be different, leading to significant 207Pb/206Pb heterogeneity on a nanometer scale within the zircon wherever Pb has been redistributed into clusters or nanospheres at some time in the past6.
Materials and Methods
Zircon grains for the present study (see sample preparation details in references9,10) came from a granulite-facies orthogneiss from Gage Ridge (rock sample 975, grains 07 and 66) in the Napier Complex of East Antarctica. At least two high-grade metamorphic events have been recognized in the area. Low-P and high-T metamorphism occurred at ca 2.8 Ga, followed by an ultra-high-temperature (UHT) event at ca 2.55 Ga, with temperature estimates as high as 1100 °C24,25,26,27 for the latter.
Four foils across grains 07 and 66 (2 foils from each) were prepared for TEM study to verify the Pb nanosphere distribution from rim to core. The site-specific focused-ion-beam (FIB) technique, which allows cutting an electron-transparent foil from pre-selected areas of interest, was applied28,29. The TEM foils were 15–20 μm wide, 10–15 μm deep and 150 nm thick. A glass fibre attached to a micro-manipulator was used to lift out foils from the excavation sites. Details of the technique are given in Wirth30. Analytical and energy-filtered high-resolution transmission electron microscopy (ATEM, HRTEM) using a FEI TecnaiTM G2 F20 X-Twin at GeoForschungs Zentrum (GFZ) in Potsdam, operated at 200 kV with a field emission gun (FEG) electron source, was used for the present study. The TEM is equipped with a post-column Gatan imaging filter (GIF Tridiem). The HRTEM images presented were energy-filtered using a 10 eV window on the zero loss peak. ATEM was performed with an EDAX X-ray analyzer equipped with an ultra-thin window. The X-ray intensities were measured in scanning transmission mode (STEM) where the electron beam was serially scanned over a pre-selected area, minimizing mass loss during data acquisition.
Previous SIMS 207Pb/206Pb dating of zircons utilized large primary ion beams (on the nA scale) and consequently spatial resolutions of ~10–20 µm were required in order to generate sufficiently large Pb+ secondary ion signals for analysis. This is a consequence of the Pb abundance averaged over the zircon being at the ppm level. However, as the Pb nanospheres are Pb metal, if the primary SIMS ion beam can be made of a similar dimension to the nanosphere, then measurable Pb+ secondary ion signals may be generated31. This is achieved by the NanoSIMS where the primary ion beam can be focused to a spatial resolution of 50–100 nm.
The University of Manchester NanoSIMS was here equipped with a duoplasmatron source for O− (minimum primary ion spot size 100 nm) and the University of Pau NanoSIMS was equipped with a RF-Plama O- ion source for high brightness and spatial resolution of 50 nm. A primary ion beam of O− was used to sputter positive secondary ions in imaging mode over areas between 100 × 100 μm2 and 1 × 1 μm2.
At ~2 × 102−1 × 106 Pb atoms per nanosphere and a detection efficiency of ~5 × 10−3 this leads to a total detected number of Pb+ ions of between ~1 to 1 × 103 per nanosphere, so the precision on measured 207Pb/206Pb from individual nanospheres will be limited by counting statistics. The detection efficiency was calibrated from the total Pb+ secondary ion current compared to the number of Pb atoms sputtered from a Pb metal standard.
The Manchester and Pau NanoSIMS are each equipped with a multicollector for the simultaneous acquisition of secondary ion beams. The highest mass at which single mass unit spacing may be achieved is 56 which meant that 204Pb+ could be measured in multicollection mode with 208Pb+, but 206Pb+ and 207Pb+ could only be measured by magnetic peak switching on a single detector. The measurement cycle in imaging mode therefore acquired 206Pb+, then 207Pb+, and then the simultaneous acquisition of 27Al+, 40Ca+, 48Ti+, 89Y+, 190HfO+, 204Pb+ and 208Pb+. This procedure was changed for some data acquisitions where detector 7 was used to acquire 206Pb in multicollection with the other species and used magnetic peak switching to acquire 207Pb. This had the advantage of more time spent on acquiring 207Pb and 206Pb but the disadvantage of not acquiring measurements of 204Pb and 208Pb. Repetition of this cycle until the nanospheres were completely sputtered away allowed the determination of 207Pb/206Pb for individual nanospheres by defining regions of interest (ROIs) around the Pb nanospheres in the isotope images and extracting counts for the different measured species. Automated algorithms for particle detection based on threshold intensity within the acquired images were used in L’Image (NanoSIMS image processing software, L Nittler) to define areas of 207Pb and 206Pb clustering. After defining the ROIs, these areas of Pb concentration were subtracted from the whole image to define a host zircon ROI which contained 207Pb and 206Pb without detectable Pb concentrations.
The data acquisition and processing procedures were tested by imaging 100 µm2 areas of a NIST 981 Pb metal standard and dividing the area into 104 100 × 100 nm2 square ROIs to obtain 204Pb/206Pb, 207Pb/206Pb and 208Pb/206Pb for each ROI. Reproducibility of Pb isotope ratios are within 11‰ for 204Pb/206Pb, 8‰ for 207Pb/206Pb and 4‰ for 208Pb/206Pb of the certified NIST 981 ratios22 and within the counting statistic errors at the 2σ level. This procedure demonstrated that the precision on acquired 204Pb/206Pb, 207Pb/206Pb and 208Pb/206Pb measurements on zircon samples was limited by counting statistics alone and that there were no systematic errors at this level of precision which affected the accuracy of the measured ratios.
An assessment was made of the initial Pb content of the zircon by measuring the abundance of 204Pb, and of 208Pb formed through the decay of 232Th and these data are presented in Table 1 in the supplementary information.
NanoSIMS depth profile
A 3-dimensional depth profile of a volume 1 μm × 0.7 μm × 0.3 μm was acquired by rastering a 50 nm diameter beam across an area of 1 μm × 1 μm and sputtering into the sample. The result is shown in Fig. 4. The image was acquired with 64 × 64 pixels = 15 nm pixel−1. Drift correction and data analysis was carried out using L’Image software (L. Nittler) and used to produce images of 87 individual sample planes with 3 pixels smoothing in each detected species to match the primary ion beam spot size. A composite image of the stack of 87 images formed by merging the images of 27Al, 48Ti and 206Pb (Fiji image analysis software, https://fiji.sc/) was used to generate the 3-dimensional image. The depth axis has been stretched by a factor of 3 to show the relative positions of these species within the volume.
Our TEM data confirm that Pb nanospheres in zircon are present regardless of zircon growth zonation, cracks or inclusions (Fig. 2). Lead nanospheres are heterogeneously distributed and of various sizes. They occur either as individual inclusions directly in the zircon host or together with a Si-rich phase (visible as a black mantle around the white Pb nanospheres in Fig. 2), locally together with an Al-Ti phase (not visible on Fig. 2). Isotope maps acquired by NanoSIMS mapping show that not only is Pb heterogeneously distributed (sharply defined nanospheres of 206Pb and 207Pb), but there is an association of 27Al and 48Ti with some of Pb nanospheres (Fig. 3). The Ca+ images (Fig. 2 in supplementary information; SI) showed a high background level, heterogeneous distribution that was interpreted as contamination of the sample surface by Ca-bearing contaminants and so is not further considered here. The distribution of 89Y reveals zonation characteristic of magmatic zircon growth. Depth profiles were obtained in order to characterize both the Pb nanospheres at the exposed surface of the grain and at depth. A 3D reconstruction of a 1 × 0.7 × 0.3 µm3 volume obtained by depth profiling a 1 µm2 area confirms the heterogeneous distribution of the Pb nanospheres both horizontally and vertically and shows that they are not only at the surface of the grain but at depth (Fig. 4). An important result from the depth profiling is that clustering of Pb does not always co-cluster with Ti and/or Al.
Compiled measurements of 207Pb/206Pb values for resolved Pb nanospheres and for Pb in the host zircon are presented in Table 1. The 204Pb/206Pb values measured in the nanospheres and in the zircon host (Table 1, SI) were typically zero, resulting from no detected counts of 204Pb within those ROIs. Detector noise counts are typically ~0.5 s−1 but in imaging mode are spread over 256 × 256 pixels, the probability of a noise count appearing within the ROI defining a nanosphere (typically 6–10 pixels) is ~10−2 over a typical data acquisition period. This allows us to place an upper limit of 204Pb/206Pb < 0.003 measured within nanospheres and assuming a 204Pb/206Pb = 0.079 in the Earth at 3 Ga, an upper limit on the amount of inherited Pb as <4%. This places an upper limit on the possible systematic error on 207Pb/206Pb in nanospheres as +0.02 due to possible inherited Pb which is smaller than the confidence limits on 207Pb/206Pb given by counting statistic precision. This demonstrates that inherited Pb from before the zircon formed in these cases were negligible, having no significant effect upon the Nanosphere Model Ages. Measurements of 208Pb/206Pb for individual zircons are also given in Table 1, SI. These are consistent with the measured Th/U = 0.05 for grain 66 and 0.06 for grain 0712. Thus, the assumptions of Eqs (1) and (2) are valid.
A weighted average of nanosphere 207Pb/206Pb yielded values of 0.495 ± 0.024 and 0.528 ± 0.030 (2σ error in the mean) and zircon host values of 0.170 ± 0.040 and 0.195 ± 0.052 (2σ error in the mean), along with an abundance ratio Pb(nanospheres)/Pb(host) = 0.45 ± 0.10 and 0.35 ± 0.10 for grains 66 and 07, respectively.
Model ages from these values are given in Table 1.
There are a number of possible systematic errors that may affect the measured 207Pb/206Pb values.
The NanoSIMS primary ion spot-size is 50–100 nm in diameter and so much larger than typical nanosphere sizes. Thus some Pb from the zircon host around the nanosphere will be analyzed along with the nanosphere, although nanospheres are spatially resolved from each other since the average separation between nanospheres is >300 nm. Some Pb+ ions will therefore be generated from the zircon host surrounding the nanosphere, but measured as if from the nanosphere, thereby altering the measured 207Pb/206Pb ratio and the relative Pb abundances of the nanospheres. Measurements of the intensity of the Pb+ signal from zircon host between nanospheres leads to an estimate that when the primary ion beam is centered on a nanosphere, the measured Pb+ signal from the surrounding zircon host within the primary ion beam spot will typically have a contribution of between 1–4% Pb+ of the nanosphere Pb+ signal. Potentially this systematic error is more significant for smaller nanospheres. To address whether this effect could significantly alter the measured 207Pb/206Pb ratios of the nanospheres, the measured 207Pb+ and 206Pb+ counts from the zircon host with the same primary ion beam spot size as on the nanosphere was subtracted from the 207Pb+ and 206Pb+ counts recorded from each nanosphere. Although this is an approximate estimate of the correction required, as the nanosphere will occupy some of the area of the primary ion spot, nevertheless most of the area sputtered by the beam when measuring a nanosphere will be on host zircon. The Pb+ signal from zircon host nm−2 is however considerably lower than from nanospheres so the estimated correction to the mean 207Pb/206Pb of all of the nanospheres shown in the supplementary information is ~1.2%. When the range of possible NMA is obtained from this corrected 207Pb/206Pb value, it raises the mean age of T1 by ~10 Ma. Although this will be a systematic error in the measured 207Pb/206Pb ratio of a nanosphere, it is nevertheless considerably smaller than the statistical error in the measurement. As the correction is an estimate and not significant to the uncertainty in the age of the nanospheres, the ages reported remain as determined from the nanosphere 207Pb/206Pb values.
If the assumption that mobilization of Pb into nanospheres completely removes Pb from the originally metamict zircon is valid, then the 207Pb/206Pb value of the latter defines the age of the Pb mobilization event (Eq. 2). The uncertainty on this age is then defined by the uncertainty in the 207Pb/206Pb value of the zircon host. A possible systematic error in this procedure is that the smallest nanospheres may not be sufficiently large to be recognized as discrete enhancements to the 206Pb+ and 207Pb+ signals compared to statistical fluctuations in the zircon host 206Pb+ and 207Pb+ signals and so cannot be recognized as nanospheres. Any small nanospheres which are therefore counted in the zircon host 207Pb/206Pb measurement may raise the mean 207Pb/206Pb value of the zircon host.
To estimate the potential contribution of small, unrecognized nanospheres to the measurement of 207Pb/206Pb of the host zircon, the measured TEM size distribution of the nanospheres in this sample may be used (inset in Fig. 2). The distribution is approximately Gaussian and has a maximum abundance at a diameter of ~7.5 nm. We estimate that a nanosphere may not be recognized as giving an enhanced signal above the zircon host when the Pb+ signal from the nanosphere is of the same magnitude as from the zircon host surrounding the nanosphere but still within the primary ion beam spot.
Typical nanospheres yielded ~500 counts in total of 206Pb+ and 207Pb+. From the relative volumes of spherical nanospheres, we may therefore estimate that a nanosphere of diameter 2 nm or less will give a Pb+ signal that would not be larger than the statistical fluctuations in the host zircon Pb+ signal. Inspecting the measured nanosphere size distribution (Fig. 2, inset), it can be seen that no nanospheres were identified of this size in the TEM images so we may place an upper limit on nanospheres <2.5 nm in diameter of <0.5% of the nanosphere population. Estimates by mass balance indicate that this potential systematic error is not significant in the analyses reported here compared to the statistical error on the zircon host 207Pb/206Pb measurement. However, this potential source of systematic error must nevertheless be evaluated for each acquisition.
Given the error limits on the measured 207Pb/206Pb values of both the zircon host and nanospheres, there are a range of possible values of T1 and T2 that will correspond to the measured values of 207Pb/206Pb. However an additional constraint may be placed on the possible combinations of values of T1 and T2 since the predicted ratio of Pb atom abundance in the nanospheres relative to those formed after the metamorphic event (which remain in the zircon host) is highly sensitive to (T1−T2). Thus, measurement of the Pb abundance in the nanospheres relative to Pb abundance in the surrounding host provides an additional powerful constraint upon the likely range of ages for these events. A significant assumption implicit in applying this constraint is that there was no Pb loss from the zircon during the Pb mobilization event at T2. Any Pb loss during this event would not have significantly altered the 207Pb/206Pb ratio of nanospheres formed at time T2 but could alter the ratio of Pb in the nanospheres to Pb formed after T2 residing in the zircon host surrounding the nanospheres.
The question arises as to the significance of the other elements that are associated with Pb mobilization in zircon from the Napier Complex in East Antarctica, namely Al, Ti and Si10. Although not the focus of the present study, it is pertinent to briefly discuss their distribution with respect to the Pb nanospheres and compare with other studies where radiogenic Pb concentrations have been recorded. The overall issue of Pb mobilization in zircon has been discussed in several papers utilizing various methods10,11,12,13,14,15,16,17,18,19,20,21, with only TEM capable of identifying crystalline metal Pb nanospheres. However, this phenomenon is not limited to zircons from the Napier Complex as metallic Pb nanospheres were also documented in the Kerala Khondalite Belt (KKB) in India17. What distinguishes Antarctic zircons from those in India is the presence of Al and Ti concentrations, whereas Pb nanospheres in the KKB only occur individually. Patchy distribution of Ti may have implications for Ti-in-zircon thermometry and Hadean tectonics12,32,33. Clustering of Al was also observed in zircons from the Napier Complex in the APT study21, where areas with increased Al content corresponded to increases of Y and U in individual dislocation arrays. This is not the case in the present study, as no correlation with Y or U occurs. The presence of Al in zircon from Jack Hills in Australia was also reported and explained as due to a high-Al source34. Furthermore, Y accumulations were also reported in association with Pb clusters in Jack Hills zircon18,19, but were not identified in the present study. This raises the issue of exactly how these various elements come to be concentrated in formerly metamict zircon. Currently, diverse mechanisms have been suggested, none of which fully explain the range of features exhibited by all known examples. Hence further work is required to solve what drives this phenomenon.
Zircon crystallization ages for grains 66 and 07 have been reported previously using conventional SIMS11. Grain 66 gave a 207Pb/206Pb age of 3344 ± 15 Ma and a 206Pb/238U age of 3162 ± 15 Ma (discordant), and grain 07 a 207Pb/206Pb age of 3609 ± 13 Ma and a 206Pb/238U age of 3705 ± 26 Ma (reversely discordant). As the Gage Ridge sample is a granulite-facies orthogneiss, it would be expected that the zircons within it were formed in situ and convergent crystallization ages between grains would be anticipated, whereas the ages determined by Kusiak et al.11, are not. The zircon formation model ages determined in this work from nanospheres were grain 66, 3225 Ma and grain 07, 3045 Ma. The range of possible crystallization ages which are consistent within the experimental measurement errors are ±150 Ma and so the two grains have ages concordant with the ages determined by conventional SIMS11 for grain 66, but not with grain 07.
A minimum age of 2.47 Ga, and probably older than 2.55 Ga, has been reported for the ultrahigh temperature metamorphic event in the Napier Complex35, consistent with the ages determined for the Pb mobilization event, grain 66 of 2560 ± 100 Ma and grain 07 2640 ± 90 Ma.
Regardless of the formation mechanism of Pb nanospheres, their potential to affect precise U-Pb age estimates must be taken into consideration12. Wherever a process such as metamorphism has resulted in Pb mobilization, there exists the capability for forming Pb clusters and/or Pb nanospheres with a frozen 207Pb/206Pb ratio and values that are significantly higher than the zircon host. Since the Pb nanospheres documented here have a mean diameter of 7.5 nm, separations of typically ~300 nm and are randomly distributed, conventional SIMS 207Pb/206Pb analysis, with an analytical spot size of 10–25 μm, would sample both Pb nanospheres and the zircon host, combining them together in unpredictable proportions. This has serious implications because recent scientific advances36 have enabled the SIMS analytical spot size to be reduced to <10 µm. However, the high resolution measurement of individual Pb nanospheres and their host zircon by NanoSIMS, as presented above, can for the first time resolve both the time of zircon formation and the metamorphic event during which the Pb was mobilized and Pb nanospheres were formed.
The data that support this study are held in University of Manchester Data Repository RDMP118 and are available on request from the corresponding author.
Wetherill, G. W. Discordant uranium-lead ages, I. Eos, Transactions American Geophysical Union 37, 320–326, https://doi.org/10.1029/TR037i003p00320 (1956).
Williams, I. S., Compston, W., Black, L. P., Ireland, T. R. & Foster, J. J. Unsupported Radiogenic Pb in Zircon - a Cause of Anomalously High Pb-Pb, U-Pb and Th-Pb Ages. Contrib Mineral Petr 88, 322–327 (1984).
Wiedenbeck, M. An Example of Reverse Discordance during Ion Microprobe Zircon Dating - an Artifact of Enhanced Ion Yields from a Radiogenic Labile Pb. Chemical Geology 125, 197–218 (1995).
Mezger, K. & Krogstad, J. Interpretation of discordant U-Pb zircon ages: An evaluation. J Metamorph Geol 15, 127–140 (1997).
Carson, C. J., Ague, J. J., Grove, M., Coath, C. D. & Harrison, T. M. U-Pb isotopic behaviour of zircon during upper-amphibolite facies fluid infiltration in the Napier Complex, east Antarctica. Earth Planet Sc Lett 199, 287–310 (2002).
Kusiak, M. A. et al. In Microstructural Geochronology: Planetary Records Down to Atom Scale, Geophysical Monograph (eds Moser, D. E. et al.) Ch. 13, 279–292 (John Wiley & Sons, Inc., 2017).
Bea, F., Montero, P. & Palma, J. F. M. Experimental evidence for the preservation of U-Pb isotope ratios in mantle-recycled crustal zircon grains. Sci Rep-Uk 8, 12904, https://doi.org/10.1038/s41598-018-30934-4 (2018).
Geisler, T., Pidgeon, R. T., van Bronswijk, W. & Kurtz, R. Transport of uranium, thorium, and lead in metamict zircon under low-temperature hydrothermal conditions. Chemical Geology 191, 141–154 (2002).
Nasdala, L. et al. Metamictisation of natural zircon: accumulation versus thermal annealing of radioactivity-induced damage. Contrib Mineral Petr 141, 125–144 (2001).
Kusiak, M. A. et al. Metallic lead nanospheres discovered in ancient zircons. Proceedings of the National Academy of Sciences of the United States of America 112, 4958–4963 (2015).
Kusiak, M. A. et al. Changes in zircon chemistry during Archean UHT metamorphism in the Napier Complex, Antarctica. American Journal of Science 313, 933–967, https://doi.org/10.2475/09.2013.05 (2013).
Kusiak, M. A., Whitehouse, M. J., Wilde, S. A., Nemchin, A. A. & Clark, C. Mobilization of radiogenic Pb in zircon revealed by ion imaging: Implications for early Earth geochronology. Geology 41, 291–294, https://doi.org/10.1130/g33920.1 (2013).
Whitehouse, M. J., Kumar, G. R. R. & Rimša, A. Behaviour of radiogenic Pb in zircon during ultrahigh-temperature metamorphism: an ion imaging and ion tomography case study from the Kerala Khondalite Belt, southern India. Contrib Mineral Petr 168, 1–18, https://doi.org/10.1007/S00410-014-1042-2 (2014).
Ge, R. et al. A 4463 Ma apparent zircon age from the Jack Hills (Western Australia) resulting from ancient Pb mobilization. Geology 46, 303–306, https://doi.org/10.1130/G39894.1 (2018).
Ge, R. et al. Mechanisms and consequences of intra-crystalline enrichment of ancient radiogenic Pb in detrital Hadean zircons from the Jack Hills, Western Australia. Earth Planet Sc Lett 517, 38–49, https://doi.org/10.1016/j.epsl.2019.04.005 (2019).
Utsunomiya, S. et al. Nanoscale occurrence of Pb in an Archean zircon. Geochimica Et Cosmochimica Acta 68, 4679–4686, https://doi.org/10.1016/J.Gca.2004.04.018 (2004).
Whitehouse, M. J., Kusiak, M. A., Wirth, R. & Ravindra Kumar, G. R. Metallic Pb nanospheres in ultra-high temperature metamorphosed zircon from southern India. Miner Petrol 111, 467–474, https://doi.org/10.1007/s00710-017-0523-1 (2017).
Valley, J. W. et al. Hadean age for a post-magma-ocean zircon confirmed by atom-probe tomography. Nat Geosci 7, 219–223, https://doi.org/10.1038/Ngeo2075 (2014).
Valley, J. W. et al. Nano- and micro-geochronology in Hadean and Archean zircons by atom-probe tomography and SIMS: New tools for old minerals. Am Mineral 100, 1355–1377 (2015).
Peterman, E. M. et al. Nanogeochronology of discordant zircon measured by atom probe microscopy of Pb-enriched dislocation loops. Science Advances 2, e1601318, https://doi.org/10.1126/sciadv.1601318 (2016).
Piazolo, S. et al. Deformation-induced trace element redistribution in zircon revealed using atom probe tomography. Nat Commun 7, 20490, https://doi.org/10.1038/ncomms10490 (2016).
Schoene, B. In Treatise on Geochemistry 2nd edition. The Crust 4 (ed. Rudnick, R. L.) 341–378 (Elsevier, 2014).
Geisler, T., Schaltegger, U. & Tomaschek, F. Re-equilibration of zircon in aqueous fluids and melts. Elements 3, 43–50 (2007).
Harley, S. L. & Motoyoshi, Y. Al zoning in orthopyroxene in a sapphirine quartzite: Evidence for >1120°C UHT metamorphism in the Napier Complex, Antarctica, and implications for the entropy of sapphirine. Contrib Mineral Petr 138, 293–307 (2000).
Kelly, N. M. & Harley, S. L. An integrated microtextural and chemical approach to zircon geochronology: refining the Archaean history of the Napier Complex, east Antarctica. Contrib Mineral Petr 149, 57–84, https://doi.org/10.1007/S00410-004-0635-6 (2005).
Harley, S. L., Kelly, N. M. & Kusiak, M. A. In Earth’s Oldest Rocks (Second Edition) (eds Martin J. Van Kranendonk, Vickie C. Bennett, & J. Elis Hoffmann) 865–897 (Elsevier, 2019).
Hokada, T., Motoyoshi, Y., Suzuki, S., Ishikawa, M. & Ishizuka, H. Geodynamic evolution of Mt. Riiser-Larsen, Napier Complex, East Antarctica, with reference to the UHT mineral associations and their reaction relations. Geological Society, London, Special Publications 308, 253–282, https://doi.org/10.1144/sp308.13 (2008).
Tsunogae, T. et al. Carbonic fluids in ultrahigh-temperature metamorphism: evidence from Raman spectroscopic study of fluid inclusions in granulites from the Napier Complex, East Antarctica. Geological Society, London, Special Publications 308, 317–332, https://doi.org/10.1144/sp308.15 (2008).
Wirth, R. Focused Ion Beam (FIB): A novel technology for advanced application of micro- and nanoanalysis in geosciences and applied mineralogy. Eur J Mineral 16, 863–876 (2004).
Wirth, R. Focused Ion Beam (FIB) combined with SEM and TEM: Advanced analytical tools for studies of chemical composition, microstructure and crystal structure in geomaterials on a nanometre scale. Chemical Geology 261, 217–229 (2009).
Hervig, R. L. et al. Useful ion yields for Cameca IMS 3f and 6f SIMS: Limits on quantitative analysis. Chemical Geology 227, 83–99, https://doi.org/10.1016/j.chemgeo.2005.09.008 (2006).
Ferry, J. M. & Watson, E. B. New thermodynamic models and revised calibrations for the Ti-in-zircon and Zr-in-rutile thermometers. Contrib Mineral Petr 154, 429–437, https://doi.org/10.1007/s00410-007-0201-0 (2007).
Ickert, R. B., Williams, I. S. & Wyborn, D. Ti in zircon from the Boggy Plain zoned pluton: implications for zircon petrology and Hadean tectonics. Contrib Mineral Petr 162, 447–461, https://doi.org/10.1007/S00410-010-0605-0 (2011).
Trail, D., Tailby, N., Wang, Y., Mark Harrison, T. & Boehnke, P. Aluminum in zircon as evidence for peraluminous and metaluminous melts from the Hadean to present. Geochemistry, Geophysics, Geosystems 18, 1580–1593, https://doi.org/10.1002/2016gc006794 (2017).
Suzuki, S., Arima, M., Williams, I. S., Shiraishi, K. & Kagami, H. Thermal history of UHT metamorphism in the Napier Complex, East Antarctica: Insights from zircon, monazite, and garnet ages. J Geol 114, 65–84 (2006).
Liu, M.-C., McKeegan, K. D., Harrison, T. M., Jarzebinski, G. & Vltava, L. The Hyperion-II radio-frequency oxygen ion source on the UCLA ims1290 ion microprobe: Beam characterization and applications in geochemistry and cosmochemistry. Int J Mass Spectrom 424, 1–9, https://doi.org/10.1016/j.ijms.2017.11.007 (2018).
This research was supported by a Humboldt Fellowship and NCN grant UMO2016/21/B/ST10/02067 (to MAK), and The Science and Technologies Facilities Council, UK grant ST/M001253/1. The University of Manchester NanoSIMS was funded by UK Research Partnership Investment Funding (UKRPIF) Manchester RPIF Round 2. This work was supported by the Henry Royce Institute for Advanced Materials, funded through EPSRC grants EP/R00661X/1, EP/S019367/1, EP/P025021/1 and EP/P025498/1. The University of Pau NanoSIMS was funded by the French National Research Agency ANR via the Equipex project ANR-11-EQPX-0027 MARSS. We thank Geoscience Australia and Chris Carson for providing samples, Greg McMahon for technical assistance and CAMECA for assistance and enabling the use of the Pau NanoSIMS whilst in the CAMECA factory.
The authors declare no competing interests.
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Lyon, I.C., Kusiak, M.A., Wirth, R. et al. Pb nanospheres in ancient zircon yield model ages for zircon formation and Pb mobilization. Sci Rep 9, 13702 (2019). https://doi.org/10.1038/s41598-019-49882-8
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