Multimethod U–Pb baddeleyite dating: insights from the Spread Eagle Intrusive Complex and Cape St. Mary's sills, Newfoundland, Canada

Abstract

Baddeleyite (${\mathrm{ZrO}}_{\mathrm{2}}$) is widely used in U–Pb geochronology but analysis and age interpretation are often difficult, especially for samples which have experienced post-intrusive alteration and/or metamorphism. Here, we combine high spatial resolution (secondary ionization mass spectrometry, SIMS) and high-precision (isotope dilution thermal ionization mass spectrometry, ID-TIMS) analyses of baddeleyite from the Spread Eagle Intrusive Complex (SEIC) and Cape St. Mary's sills (CSMS) from Newfoundland. Literature data and our own detailed microtextural analysis suggest that at least seven different types of baddeleyite–zircon intergrowths can be distinguished in nature. These include secondary baddeleyite inclusions in altered zircon, previously unreported from low-grade rocks, and likely the first discovery of xenocrystic zircon inclusions mantled by baddeleyite. ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ baddeleyite dates from SIMS and ID-TIMS mostly overlap within uncertainties. However, some SIMS sessions of grain mounts show reverse discordance, suggesting that bias in the U $/$ Pb relative sensitivity calibration affected ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates, possibly due to crystal orientation effects, and/or alteration of baddeleyite crystals, which is indicated by unusually high common-Pb contents. ID-TIMS data for SEIC and CSMS single baddeleyite crystals reveal normal discordance as linear arrays with decreasing ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates, indicating that their discordance is dominated by recent Pb loss due to fast pathway diffusion or volume diffusion. Hence, ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates are more reliable than ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates even for Phanerozoic baddeleyite. Negative lower intercepts of baddeleyite discordia trends for ID-TIMS dates for SEIC and CSMS and direct correlations between ID-TIMS${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates and the degree of discordance may indicate preferential ${}^{\mathrm{206}}\mathrm{Pb}$ loss, possibly due to ${}^{\mathrm{222}}\mathrm{Rn}$ mobilization. In such cases, the most reliable crystallization ages are concordia upper intercept dates or weighted means of the least discordant${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates.

We regard the best estimates of the intrusion ages to be $\mathrm{498.7}\pm \mathrm{4.5}$ Ma (2$\mathit{\sigma }$; ID-TIMS upper intercept date for one SEIC dike) and $\mathrm{439.4}\pm \mathrm{0.8}$ Ma (ID-TIMS weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date for one sill of CSMS). This first radiometric age for the SEIC is consistent with stratigraphic constraints and indicates a magmatic episode prior to opening of the Rheic Ocean. Sample SL18 of the Freetown Layered Complex (FLC), Sierra Leone, was investigated as an additional reference. For SL18, we report a revised $\mathrm{201.07}\pm \mathrm{0.64}$ Ma intrusion age, based on a weighted mean${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date of previous and new baddeleyite ID-TIMS data, agreeing well with corresponding SIMS data. Increasing discordance with decreasing crystal size in SL18 indicates that Pb loss affected baddeleyite rims more strongly than cores. Our SL18 results validate that the SIMS in situ approach, previously used for Precambrian and Paleozoic samples, is also suitable for Mesozoic baddeleyite.

1 Introduction

Baddeleyite, a monoclinic ${\mathrm{ZrO}}_{\mathrm{2}}$ polymorph, is one of the most commonly used minerals in U–Pb geochronology, especially for mafic rocks, which are traditionally difficult to date (e.g., Schaltegger and Davies, 2017). It forms most readily during the late stage of igneous crystallization from a silica-undersaturated residual melt and can coexist with zircon at conditions near silica saturation (Heaman and LeCheminant, 1993; Schaltegger and Davies, 2017). Where both minerals coexist, geochronologists have tended to prefer baddeleyite dates because it is (1) a primary igneous mineral, facilitating age interpretation; (2) rarely inherited from country rock; and (3) more resistant to Pb loss compared to zircon (e.g., Heaman and LeCheminant, 1993), as it remains crystalline even at high radiation doses (Lumpkin, 1999). U–Pb baddeleyite dating has proved powerful in solving numerous problems in earth and planetary sciences (e.g., Olsson et al., 2011; Moser et al., 2013; Wall and Scoates, 2016; Davies et al., 2017; White et al., 2020).

However, many of these studies were able to work with rather large, texturally simple, unaltered and concordant baddeleyite crystals. Such favorable conditions are the exception rather than the rule for large parts of the geologic record. In fact, crystals are often too small for mineral separation (Söderlund and Johansson, 2002), prohibiting high-precision ID-TIMS (isotope dilution-thermal ionization mass spectrometry) analysis. Instead, they can be analyzed in situ by secondary ionization mass spectrometry (SIMS; e.g., Schmitt et al., 2010; Chamberlain et al., 2010) or laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS; e.g., Renna et al., 2011). In situ methods require relative sensitivity corrections, which may be complicated by crystal orientation effects (Wingate and Compston, 2000), although these effects for SIMS can be reduced by oxygen flooding (Schmitt et al., 2010; Li et al., 2010). Furthermore, baddeleyite can be intergrown with other Zr-bearing minerals, especially in rocks with a metamorphic or hydrothermal overprint, where fluids with high ${\mathrm{SiO}}_{\mathrm{2}}$ activity often cause partial reaction of baddeleyite to polycrystalline zircon (Heaman and LeCheminant, 1993; Söderlund et al., 2013). In situ dating after careful micropetrographic investigation can resolve such intergrowths, and for ID-TIMS, baddeleyite can be selectively dissolved in hydrochloric acid, leaving zircon rims essentially undissolved (Rioux et al., 2010). However, even baddeleyite that lacks zircon intergrowths is often discordant and chemical abrasion, which is now routinely used to produce more concordant zircon data, is ineffective for reducing baddeleyite discordance (Rioux et al., 2010). Mechanisms such as alpha recoil (Davis and Sutcliffe, 1985; Davis and Davis, 2018), Pb loss due to fast pathway diffusion (Rioux et al., 2010; Söderlund et al., 2013; Schaltegger and Davies, 2017), and isotopic disequilibrium due to ${}^{\mathrm{231}}\mathrm{Pa}$ excess (Amelin and Zaitsev, 2002; Crowley and Schmitz, 2009) or ${}^{\mathrm{222}}\mathrm{Rn}$ loss (Heaman and LeCheminant, 2000) have been proposed to explain baddeleyite discordance, but none of these are universally accepted as the dominant baddeleyite discordance mechanism.

It is necessary to investigate to which degree reliable baddeleyite dating is possible when several of the abovementioned challenges come together. Here, we present a case study of dating the Spread Eagle Intrusive Complex (SEIC) and Cape St. Mary's sills (CSMS) of the Avalon Zone of Newfoundland. These early Paleozoic mafic dikes and sills were affected by low-grade metamorphism and contain abundant texturally complex baddeleyite, as commonly found in the geologic record. Moreover, the approximate intrusion age of the SEIC is constrained by its stratigraphic context. We applied U–Pb geochronology by SIMS and ID-TIMS on the same baddeleyite crystals, combined with detailed micropetrographic characterization of baddeleyite by scanning electron microscopy (SEM) before and after SIMS analysis. Our comparison of SIMS and ID-TIMS dating also includes essentially unaltered baddeleyite from the Duluth gabbro (sample FC-4b; Schmitt et al., 2010) and Freetown Layered Complex (sample SL18; Callegaro et al., 2017), leading to a critical evaluation of possibilities and limitations in dating small, texturally complex and/or altered baddeleyite crystals. Based on our micropetrographic and geochronologic data, we discuss various types of baddeleyite–zircon intergrowths, possible mechanisms of baddeleyite discordance and the reliability of different types of baddeleyite dates (e.g., ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$, ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$, concordia upper intercept). Many of these implications are also significant for unaltered baddeleyite.

Figure 1

Simplified geological map of the western Avalon Peninsula, compiled after King (1988) and O'Brien et al. (2001).

[Figure omitted. See PDF]

2 Regional geology

The Avalon Peninsula consists of rocks that were formed as part of the microcontinent Avalonia during the Neoproterozoic and early Paleozoic (e.g., Williams, 1979; Murphy et al., 1999; Fig. 1). The Cambrian Adeyton and Harcourt groups (Hutchinson, 1962; King, 1988; Fig. 2), which unconformably overlie Precambrian rocks, consist of well-preserved marine sediments with intercalated pillow basalts and mafic tuffs. The feeder pipes or dike-like conduits of these volcanic rocks make up a mafic intrusive complex, called the “Spread Eagle Gabbro” (McCartney, 1967) or “Spread Eagle Gabbro and equivalents“ (King, 1988). To avoid confusion, we define this unit, consisting of at least 11 dikes, as the Spread Eagle Intrusive Complex (SEIC). Lower Ordovician sedimentary rocks are exposed only on Conception Bay islands northeast of the study area (King, 1988). They are roughly coeval with Avalonia's presumably early Ordovician separation from Gondwana (e.g., Cocks et al., 1997; Murphy et al., 2006; Linnemann et al., 2008, 2012; Pollock et al., 2009, 2012). The Cambrian pillow basalts and their feeder dikes are confined to the western Avalon Peninsula, which experienced deformation and pervasive low-grade metamorphism during the Acadian Orogeny (McCartney, 1967), lasting from ca. 420 to 360 Ma (van Staal and Barr, 2012; Willner et al., 2014).

2.1 Spread Eagle Intrusive Complex (SEIC) and Cambrian volcanic rocks

Cambrian shales of the Chamberlain's Brook Formation and Manuels River Formation contain pillow basalt flows and/or basaltic metatuffs in five different localities (McCartney, 1967; Greenough, 1984; Greenough and Papezik, 1985b; Fletcher, 2006). Additionally, our field observations suggest their presence also within the overlying Elliot Cove formation (sensu stricto King, 1988). Several lines of indirect field evidence substantiate that these volcanic rocks were fed by the SEIC dikes or pipes which crop out in their vicinity (Greenough, 1984; Greenough and Papezik, 1985b). The SEIC intrusions are arranged in a N–S-trending array (Fig. 1) and are usually subcircular pipes with diameters of several hundreds of meters (McCartney, 1967). Petrologically, they are internally differentiated, ranging from melanogabbros to leucogabbros (Greenough, 1984; Greenough and Papezik, 1985b) and monzonites (this study). These subvolcanic rocks are considerably altered to a greenschist facies assemblage but better preserved than the volcanic rocks, which almost completely lack primary minerals (Greenough and Papezik, 1985a, b). Geochemical features of the SEIC rocks are similar to rift basalts, suggesting that Avalonia experienced extensional tectonics in the Cambrian (Greenough and Papezik, 1985b; Greenough and Papezik, 1986a; new whole-rock major and trace-element data are given in the Sect. S7). Early attempts at radiometric dating of the SEIC failed, as alteration hampered Rb–Sr whole-rock methods and zircons were not found (Greenough, 1984). Samples of the current study were collected from several SEIC feeder pipes (Table 1).

Figure 2

Cambrian stratigraphy of the western Avalon Peninsula, compiled after King (1988), Fletcher (2006) and Austermann (2016). Subdivision of the Cambrian after Peng et al. (2012).

[Figure omitted. See PDF]

Table 1

Samples used for U–Pb geochronology.

Unit	Sample	Coordinates	Rock type	Typical crystal size ($\mathrm{\mu }$m)		SIMS		ID-TIMS
				Baddeleyite	Zircon	In situ	Grain mount
SEIC	FP6D	47${}^{\circ }$22.004${}^{\prime }$ N, 053${}^{\circ }$39.802${}^{\prime }$ W	Pegmatoidal monzonite	50–200	50		X	X
	FP7G	47${}^{\circ }$22.098${}^{\prime }$ N, 053${}^{\circ }$39.178${}^{\prime }$ W	Monzogabbro	5–30	5–10	X
	FP12A	47${}^{\circ }$31.274${}^{\prime }$ N, 053${}^{\circ }$39.259${}^{\prime }$ W	Gabbro	10–30	5–10	X
CSMS	S2C	46${}^{\circ }$47.756${}^{\prime }$ N,	Granophyre	Inclusions	20–200	X
		054${}^{\circ }$05.866${}^{\prime }$ W		in zircon
	S2E	46${}^{\circ }$47.756${}^{\prime }$ N, 054${}^{\circ }$05.866${}^{\prime }$ W	Granophyre	5–200	50–200	X	X	X
Duluth gabbro	FC-4b	47${}^{\circ }$46.118${}^{\prime }$ N, 091${}^{\circ }$21.402${}^{\prime }$ W	Gabbroic anorthosite	100–200	100–200	X		X${}^{*}$
FLC	SL18	08${}^{\circ }$27${}^{\prime }$ N, 13${}^{\circ }$13${}^{\prime }$ W	Olivine gabbronorite	tens to hundreds	–	X	X	X${}^{*}$

${}^{*}$ ID-TIMS data for FC-4b are from Schmitt et al. (2010); those for SL18 are partly from Callegaro et al. (2017).

2.2 Cape St. Mary's sills (CSMS)

In addition to the occurrence of the Cambrian igneous rocks described above, the Cambrian succession is intruded by the CSMS in the southwestern Avalon Peninsula, especially in the upper Cambrian Gull Cove Formation (Fletcher, 2006). The sills are up to 60 m thick and consist mostly of gabbro, but the thickest sills also include up to 3 m thick granophyric dikes and pockets (Greenough and Papezik, 1986b; Fletcher, 2006). The gabbros and granophyres are both unusually rich in hydrous minerals, notably amphibole and biotite, and volatile complexing was probably an important differentiation process of the subalkaline parental magma (Greenough and Papezik, 1986b). Trace-element patterns indicate that the magma was generated from a mantle source that had been metasomatically enriched by subduction-zone-derived fluids (Greenough et al., 1993; this study, Supplement Sect. S7). A CSMS granophyre was the first terrestrial rock for which baddeleyite dating was performed (Greenough, 1984 and John D. Greenough, personal communication, 2019). These ID-TIMS analyses of multiple-crystal aliquots yielded an early Silurian weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date of $\mathrm{441}\pm \mathrm{2}$ Ma, but all analyses are discordant to 2.0 %–3.5 % (Greenough et al., 1993). Combining this date with a paleolatitude of 32${}^{\circ }$ S $\pm$ 8${}^{\circ }$, the CSMS was interpreted as the result of an igneous event after Avalonia's separation from Gondwana but before complete closure of the Iapetus Ocean (Hodych and Buchan, 1998). Samples of the current study were collected from a 60 m thick sill at the southwestern coast of Lance Cove (Table 1) from the same sill as in Greenough et al. (1993).

3 U–Pb geochronology methods

Care was taken during field work to collect samples as coarse-grained and unaltered as possible. Such samples are most likely to yield large high-quality baddeleyite crystals, as baddeleyite typically forms in interstitial melt pockets and can react to zircon in response to Si-bearing metamorphic fluids (Heaman and LeCheminant, 1993). Polished thin sections of selected samples were investigated by SEM (backscattered electron (BSE) and cathodoluminescence (CL) imaging and energy dispersive X-ray spectrometry (EDS)) to localize baddeleyite and study its textural properties. When baddeleyite and/or zircon crystals were too small for mineral separation ($<$ 50 $\mathrm{\mu }$m), they were analyzed in situ in thin section by SIMS for U–Pb dates (Table 1). For samples with larger crystals, polished epoxy grain mounts were prepared from handpicked separates, followed by SEM imaging and SIMS analysis. Every SIMS session was followed by re-imaging of the analysis craters by SEM to identify analyses with contributions from adjacent phases (see Supplement Sect. S1). Selected crystals were removed from grain mounts for single-crystal ID-TIMS analyses.

SIMS analyses were performed using a CAMECA ims1280-HR ion probe at Heidelberg University. Oxygen flooding of the sample chamber was employed to mitigate crystal orientation effects and improve secondary ion yields (Schmitt et al., 2010; Chamberlain et al., 2010; Li et al., 2010), using oxygen pressures of 2.0–$\mathrm{3.0}\times {\mathrm{10}}^{-\mathrm{3}}$ Pa. The primary ion beam was focused to a diameter of about 10–15 $\mathrm{\mu }$m. In cases where an even higher spatial resolution was needed, the field aperture of the secondary beam was closed to a square of 5–8 $\mathrm{\mu }$m. Analytical procedures for baddeleyite and zircon were adapted from Schmitt et al. (2010). The $\mathrm{U}/\mathrm{Pb}$ relative sensitivity calibration (RSC) against the ${\mathrm{UO}}_{\mathrm{2}}/\mathrm{U}$ ratio accounts for differences in Pb ionization caused by spot-to-spot differences in sputtering behavior. For this, Phalaborwa baddeleyite (Heaman, 2009) was always used as primary reference material. For grain mount sessions, FC-4b baddeleyite (Schmitt et al., 2010) was included as secondary reference material. Zircon analyses were calibrated using the reference materials AS3 (Schmitz et al., 2003) for U–Pb ages and 91500 (Wiedenbeck et al., 2004) for U concentrations. Zirconolite from sample FP7G was analyzed to investigate the influence of its matrix on U–Pb baddeleyite dates when the primary ion beam overlaps onto both minerals.

For ID-TIMS analyses of samples FP6D and S2E, baddeleyite dissolution and chemistry were adapted from Rioux et al. (2010). Baddeleyite crystals were plucked from the SIMS grain mount, spiked with a mixed ${}^{\mathrm{205}}\mathrm{Pb}{/}^{\mathrm{233}}\mathrm{U}{/}^{\mathrm{235}}\mathrm{U}$ tracer (ET535) and dissolved in HCl acid. Solutions were pipetted into beakers to separate them from undissolved zircon domains. Pb and ${\mathrm{UO}}_{\mathrm{2}}$ from baddeleyite were loaded onto single rhenium filaments with silica gel without ion exchange cleanup. Isotopic compositions were measured on a Micromass Sector 54 TIMS at the University of Wyoming in single Daly photomultiplier mode. The model of Stacey and Kramers (1975) at 400 Ma was used for common-Pb corrections of SIMS and ID-TIMS analyses. The decay constants and ${}^{\mathrm{238}}\mathrm{U}{/}^{\mathrm{235}}\mathrm{U}$ ratio are from Steiger and Jäger (1977). Concordia coordinates and uncertainties were calculated using IsoplotR for SIMS (Vermeesch, 2018) and PBMacDAT and IsoplotEX for ID-TIMS (Ludwig, 1988, 2003).

Secondary reference baddeleyite from the Duluth gabbro and Freetown Layered Complex (FLC)

Reference baddeleyite FC-4b is from the anorthositic series of the Duluth Complex, part of the middle Proterozoic (ca. 1.1 Ga) North American Midcontinent Rift system (Paces and Miller, 1993). This sample from the anorthositic series of the complex is described as an olivine-phyric gabbroic anorthosite (Hoaglund, 2010). FC-4b baddeleyite has yielded dates of $\mathrm{1096.84}\pm \mathrm{0.45}$ Ma (${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$; all uncertainties quoted in the text are 2$\mathit{\sigma }$) and $\mathrm{1099.6}\pm \mathrm{1.5}$ Ma (${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$) by ID-TIMS analysis (Schmitt et al., 2010). Our new SIMS data for FC-4b are from baddeleyite crystals with petrographic properties comparable to those of Schmitt et al. (2010).

Sample SL18 is an olivine gabbronorite from the Freetown Layered Complex (FLC) in Sierra Leone, which is part of the Central Atlantic Magmatic Province (CAMP). SL18 consists of plagioclase and augite with minor olivine and accessory baddeleyite and apatite. Large baddeleyite crystals (with U contents of 1–4 ng) produced a weighted mean ${}^{\mathrm{206}}\mathrm{Pb}{-}^{\mathrm{238}}\mathrm{U}$ date of $\mathrm{198.777}\pm \mathrm{0.047}$ Ma by ID-TIMS (Callegaro et al., 2017). However, these data show some scatter and the mean date was generated by 7 out of a total of 11 analyses and is still significantly younger than all zircon U–Pb ID-TIMS dates from CAMP samples (Blackburn et al., 2013; Davies et al., 2017) at $\sim$ 201.5 Ma. However, the ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date for SL18 is $\mathrm{201.19}\pm \mathrm{0.69}$ Ma, overlapping with Ar–Ar dates from FLC and U–Pb dates from CAMP samples throughout different localities. The young and slightly scattered ${}^{\mathrm{206}}\mathrm{Pb}{-}^{\mathrm{238}}\mathrm{U}$ date with an older “CAMP”-type ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ age suggests that SL18 baddeleyite may have been affected by Pb loss. Callegaro et al. (2017) discussed different age interpretations of SL18 extensively but were unfortunately unable to determine a robust U–Pb crystallization age. We present additional single-crystal ID-TIMS data of SL18, obtained with exactly the same methodology as for Callegaro et al. (2017) at the University of Geneva (details in Sect. S2) but with baddeleyite crystals from the same separate that are 10–30 times smaller.

Figure 3

Backscatter electron (BSE) images of accessory minerals in the SEIC. (a) Baddeleyite (Bad) clusters surrounded by zircon (Zrn) from sample FP1F. (b–d) Mineral separates of baddeleyite from sample FP6D, showing variable proportions of zircon domains. (e) Baddeleyite with thin zircon rims from sample FP7G. (f) Baddeleyite–zirconolite (Znl) intergrowth from sample FP7G. (g) Baddeleyite and zirconolite surrounded by zircon and titanite (Ttn).

[Figure omitted. See PDF]

Figure 4

BSE and cathodoluminescence (CL; j) images of baddeleyite–zircon intergrowths in SEIC sample FP12A. (a–d) Baddeleyite of different habits, intergrown with variable proportions of zircon. (e–l) Baddeleyite with zircon inclusions and notches.

[Figure omitted. See PDF]

4 Petrography

4.1 Spread Eagle Intrusive Complex (SEIC)

The SEIC rocks have well-preserved igneous textures, but major and accessory minerals are frequently replaced by parageneses indicative of alteration and low-grade metamorphism. Grain size and color index can vary considerably, ranging from fine-grained melanogabbros to coarser-grained rarely pegmatoidal monzonites and monzosyenites. Plagioclase is always completely altered to albite. Many samples also contain large amounts of K-feldspar. In the less potassic samples, K-feldspar is concentrated in interstitial areas or leucocratic pockets, often together with accessory minerals. Minor quartz is often present in baddeleyite-bearing and baddeleyite-free rocks but usually in secondary pockets and veins. Clinopyroxene is replaced by chlorite to a variable extent, often as pseudomorphs. Some samples have essentially unaltered clinopyroxene but also contain chlorite pseudomorphs. Ilmenite is largely replaced by titanite $\pm$ rutile $\pm$ magnetite. Other common secondary minerals are calcite, epidote, prehnite and/or pumpellyite, as well as accessory sulfides (pyrite, chalcopyrite, galena, sphalerite). Apatite is ubiquitous.

All samples contain Zr-bearing accessory phases. Baddeleyite occurs in many samples, usually as $<$ 20 $\mathrm{\mu }$m long, lath-shaped euhedral crystals. Crystals 20–80 $\mathrm{\mu }$m in length occasionally occur in some samples, and FP6D is the only sample with large (50–200 $\mathrm{\mu }$m) baddeleyite crystals (Fig. 3b–d). SEIC baddeleyite is commonly intergrown with zircon, forming a variety of textures. The most common case is that baddeleyite crystals contain zircon domains mostly at their rim but commonly penetrating into the core. This largely pseudomorphic replacement texture is accompanied by feather-like zircon coronas around the crystal (e.g., Fig. 4d). Baddeleyite preservation tends to be better if the rock is less altered but also if crystals are large, as the presence of rather modest zircon overgrowths in the strongly altered monzonite FP6D indicates. Baddeleyite inclusions in K-feldspar usually lack zircon intergrowths. In samples FP1F and FP1I, clusters of baddeleyite needles are enclosed by zircon crystals (Fig. 3a). The enclosing zircon is sometimes almost euhedral but often with feather-like zircon overgrowths. A special feature we identified in FP12A is that some baddeleyite crystals have zircon inclusions up to 3 $\mathrm{\mu }$m wide and at most 12 $\mathrm{\mu }$m long (Fig. 4f–k). Secondary zircon overgrowth on the enclosing baddeleyite was rarely observed. Besides that, FP12A contains prismatic euhedral baddeleyite crystals essentially free of zircon but with a notch on one prism plane that penetrates into the crystal's core (Fig. 4e, l). Zircon crystals without baddeleyite intergrowth are sometimes present also in baddeleyite-bearing rocks. Some of these crystals have an amoeboid surface and a scarred interior. Baddeleyite-free rocks are often either melanocratic or rich in quartz. They contain zircon as the only Zr-bearing mineral, forming euhedral ($\le$ 20 $\mathrm{\mu }$m) or anhedral ($\le$ 50 $\mathrm{\mu }$m) crystals. Only one sample (FP7G) contains zirconolite ${\mathrm{CaZrTi}}_{\mathrm{2}}{\mathrm{O}}_{\mathrm{7}}$ (all mineral formulae given as stochiometric end-members from Anthony et al., 2001) and rare pyrochlore $(\mathrm{Ca},\mathrm{Na}{)}_{\mathrm{2}}{\mathrm{Nb}}_{\mathrm{2}}{\mathrm{O}}_{\mathrm{6}}(\mathrm{OH},\mathrm{F})$ in addition to baddeleyite and zircon. Zirconolite occurs mainly in the vicinity of baddeleyite crystals of similar size and form (Fig. 3f). It sometimes has an altered appearance and/or significant Si contents. In rare cases it is partly replaced by titanite $+$ zircon (Fig. 3g).

Figure 5

BSE and CL images of accessory minerals in CSMS. (a–i) Different habits of zircon in sample S2C, most of them with baddeleyite inclusions. (j–l) Euhedral baddeleyite with and without zircon intergrowth. (m) Relict baddeleyite within zircon pseudomorph, with a feather-like zircon corona. (n) Baddeleyite and zirconolite, intergrown with zircon and gittinsite. (o) Gittinsite–titanite intergrowth within chlorite.

[Figure omitted. See PDF]

4.2 Cape St. Mary's sills (CSMS)

CSMS gabbros are less altered than those of the SEIC. Sample S2B represents a typical CSMS gabbro regarding major phase mineralogy (clinopyroxene, albite, titanomagnetite, partly chloritized biotite, chlorite pseudomorphs) and has ilmenite, Cr spinel, ilvaite ${\mathrm{CaFe}}_{\mathrm{2}}^{\mathrm{2}+}{\mathrm{Fe}}^{\mathrm{3}+}{\mathrm{Si}}_{\mathrm{2}}{\mathrm{O}}_{\mathrm{7}}\mathrm{O}\left(\mathrm{OH}\right)$ and sulfides as minor to accessory phases. Baddeleyite is the predominant Zr-bearing mineral, coexisting with zirconolite and minor zircon. Habits of baddeleyite vary from euhedral to anhedral and are needle-shaped ($\mathrm{2}\mathrm{\mu }\mathrm{m}\times \mathrm{300}$ $\mathrm{\mu }\mathrm{m}$) to prismatic ($\mathrm{10}\mathrm{\mu }\mathrm{m}\times \mathrm{20}$ $\mathrm{\mu }$m). Zircon rims are rare.

Table 2

Summary of U–Pb SIMS results (see Tables S1–S6 for the detailed data).

		${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$	$\pm \mathrm{2}\mathit{\sigma }$	$\pm \mathrm{2}\mathit{\sigma }$${}^{\text{a}}$	MSWD	${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$	$\pm \mathrm{2}\mathit{\sigma }$	MSWD
Session	$n^{\text{b}}$	date (Ma)				date (Ma)
FP6D gm baddeleyite1	24 (20)	516.2	14.9	21.2	2.03	500.8	18.0	0.54
FP6D gm baddeleyite2	30 (30)	531.9	14.1		0.38	502.5	8.6	0.83
FP6D gm baddeleyite3	28 (27)	563.4	13.6	15.2	1.25	484.1	13.5	0.65
Sessions 1–3		539.1	8.3	10.1	1.48	497.0	6.8	0.75
FP6D gm zircon	10 (4)	142–517	–		–	247–678	–	–
FP7G ins baddeleyite1	10 (4)	544.7	46.8		0.39	511.3	81.8	0.43
FP7G ins baddeleyite2	16 (7)	526.0	24.2		0.43	444.1	163.4	0.20
Sessions 1–2		529.9	21.4		0.42	497.8	73.2	0.30
FP7G ins zircon	1 (1)	263.8	11.5		–	732	432	–
FP12A ins baddeleyite1	16 (8)	509.6	11.8	17.5	2.19	479	111	0.39
FP12A ins baddeleyite2	6 (4)	527.5	63.0		0.91	725	160	0.54
FP12A ins baddeleyite3	6 (4)	468.2	53.6		0.95	520	264	0.05
FP12A ins baddeleyite4	5 (2)	505.7	62.6	83.0	1.76	418	346	1.30
Sessions 1–4		508.2	11.2	13.7	1.49	546.6	83.6	0.76
FP12A ins zircon${}^{\text{c}}$	6 (3)	311–408	–		–	325–417	–	–
S2C ins zircon	23 (13)	426.8	26.4		0.46	373.6	48.4	0.88
S2E ins baddeleyite	24(21)	446.6	12.8	15.4	1.44	436.5	21.2	0.82
S2E gm baddeleyite	42 (39)	491.0	19.8		0.45	425.5	8.7	1.00
S2E ins zircon	5 (1)	402.0	51.2		–	846	340	–
S2E gm zircon	8 (7)	411–443	–		–	282–443	–	–
SL18 ins baddeleyite	41 (34)	201.2	3.2	7.2	5.05	180.2	66.0	0.21
SL18 gm baddeleyite	61 (61)	202.5	2.2		0.78	184.3	12.5	0.79

ins represents in situ, gm represents grain mount. ${}^{\text{a}}$2$\mathit{\sigma }$ uncertainty multiplied with the square root of the MSWD (mean square weighted deviation) for samples with MSWD $>$ 1; ${}^{\text{b}}$number in parentheses is without analyses that have high common Pb ($<$ 90 % radiogenic ${}^{\mathrm{206}}\mathrm{Pb}$) or contain contributions from other U-bearing minerals. These analyses are excluded from weighted mean calculations. For zircon, a range of dates is given instead of weighted means, as the crystals may belong to several generations and/or have undergone strongly variable Pb loss. ${}^{\text{c}}$ not including zircon inclusions in baddeleyite. Analyses were acquired during sessions FP12A baddeleyite1–3.

In contrast to the gabbros, granophyres are strongly leucocratic ($>$ 70 vol % albite). Albite crystals are typically 1 $\mathrm{cm}$ $\times$ 0.5 cm large in the interior of granophyre pockets, whereas the outermost ca. 5 cm of the pockets are somewhat less leucocratic with smaller albite crystals. Nonetheless, a strong contrast of grain size and mineralogy characterizes the sharp contact between gabbros and granophyre pockets. Granophyre samples S2C (center of a pocket) and S2E (transition of a pocket center to the gabbro contact) are largely identical in major phases (albite, clinopyroxene, ilmenite, chlorite, biotite $\pm$ Ti-rich hornblende). However, the accessory mineral assemblages are highly different. In S2C, zircon is the only Zr-bearing phase with contact to groundmass minerals. Crystals are up to 200 $\mathrm{\mu }$m large, isometrical and growth zoned. Shapes vary from euhedral sector zoned with radial cracks in the outer zones (Fig. 5c) over grain clusters (Fig. 5f) to fan-shaped forms (Fig. 5i). BSE and CL intensities are usually inversely correlated (Fig. 5f, g). Some crystals have partly microporous textures and contain anhedral baddeleyite inclusions (mostly $<$ 2 $\mathrm{\mu }$m, max. $\mathrm{4}\mathrm{\mu }\mathrm{m}\times \mathrm{10}$ $\mathrm{\mu }$m in size), usually in the outer zones. Sometimes the inclusions seem to retrace cracks or crystallographical orientations (Fig. 5e). In S2E, the pocket interior has large (up to 200 $\mathrm{\mu }$m) zircon crystals but without baddeleyite inclusions, whereas baddeleyite sometimes forms isolated crystals in the groundmass. Towards the gabbro contact, baddeleyite becomes more and more predominant until the presence of zircon is mostly confined to baddeleyite replacement textures. Near the gabbro contact, baddeleyite occurs either as euhedral lath-shaped crystals with dimensions up to $\mathrm{20}\mathrm{\mu }\mathrm{m}\times \mathrm{300}$ $\mathrm{\mu }$m (Fig. 5j) or as short prismatic crystals up to 30 $\mathrm{\mu }$m in diameter (Fig. 5k). Baddeleyite within albite usually lacks zircon intergrowths. Contrastingly, most baddeleyite within chlorite pseudomorphs is pseudomorphically replaced by zircon, sometimes containing baddeleyite relicts, and surrounded by a feather-like zircon corona (Fig. 5m). Near the gabbro contact, zircon with amoeboidal grain boundaries occurs, as well as zirconolite and gittinsite ${\mathrm{CaZrSi}}_{\mathrm{2}}{\mathrm{O}}_{\mathrm{7}}$. Gittinsite has not been reported from similar rock types before. Textures include gittinsite–zirconolite intergrowths (Fig. 5n) and gittinsite–titanite intergrowths branching along the fissure plains of surrounding chlorite (Fig. 5o).

Figure 6

SIMS U–Pb baddeleyite and zircon results for SEIC samples. Ellipses in red represent analyses of baddeleyite with zircon inclusions (e) or zircon analyses with $<$ 90 % radiogenic ${}^{\mathrm{206}}\mathrm{Pb}$ (d, f). Error ellipses of individual analyses are $\mathrm{1}\mathit{\sigma }$, whereas the weighted mean ellipse (blue) is enlarged to $\mathrm{2}\mathit{\sigma }$.

[Figure omitted. See PDF]

Figure 7

SIMS U–Pb baddeleyite (a, b) and zircon (c) results for CSMS samples. Error ellipses of individual analyses (only those used for weighted mean date calculations are shown) are $\mathrm{1}\mathit{\sigma }$, whereas the weighted mean ellipse (blue) is enlarged to $\mathrm{2}\mathit{\sigma }$.

[Figure omitted. See PDF]

5 U–Pb results

5.1 SIMS data

The SEIC SIMS data are presented in Fig. 6 (summary in Table 2; detailed data in Tables S1–S6 in the Supplement). In situ baddeleyite analyses of sample FP7G yielded weighted mean dates of $\mathrm{529.9}\pm \mathrm{21.4}$ Ma (${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$) and $\mathrm{497.8}\pm \mathrm{73.2}$ Ma (${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$). For FP12A baddeleyite, the weighted mean dates are $\mathrm{508.2}\pm \mathrm{11.2}$ Ma (${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$) and $\mathrm{546.6}\pm \mathrm{83.6}$ Ma (${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$). Many baddeleyite analyses show surprisingly high contents of common Pb; those with $<$ 90 % radiogenic ${}^{\mathrm{206}}\mathrm{Pb}$ were generally excluded from weighted mean calculations. During grain mount sessions, FC-4b baddeleyite was analyzed as a secondary reference in addition to Phalaborwa baddeleyite. Weighted mean ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates of FC-4b calculated with Phalaborwa reference are $\mathrm{1118}\pm \mathrm{39}$ Ma (MSWD $=$ 0.63; $n=\mathrm{28}$), $\mathrm{1101}\pm \mathrm{44}$ Ma (MSWD $=$ 0.41; $n=\mathrm{29}$), $\mathrm{1124}\pm \mathrm{56}$ Ma (MSWD $=$ 0.91; $n=\mathrm{9}$) and $\mathrm{1117}\pm \mathrm{23}$ Ma (MSWD $=$ 2.42; $n=\mathrm{18}$; session with sample S2E). Therefore, in all grain mount sessions, the ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ ID-TIMS reference age of FC-4b ($\mathrm{1096.84}\pm \mathrm{0.45}$ Ma; Schmitt et al., 2010) was reproduced within error limits. Likewise, the ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates we obtained for Phalaborwa ($\mathrm{2058.8}\pm \mathrm{0.7}$ Ma, MSWD $=$ 6.3, $n=\mathrm{254}$) and FC-4b baddeleyite ($\mathrm{1096.0}\pm \mathrm{2.9}$ Ma, MSWD $=$ 1.1, $n=\mathrm{84}$) are in good agreement with the ID-TIMS ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ data ($\mathrm{2059.6}\pm \mathrm{0.35}$ Ma; Heaman, 2009; and $\mathrm{1099.6}\pm \mathrm{1.5}$ Ma; Schmitt et al., 2010). Because of the consistency of Phalaborwa and FC-4b results, analyses from both reference materials were combined for obtaining the U $/$ Pb relative sensitivity factor. Despite the good agreement of ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates of the reference baddeleyite, ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates of baddeleyite from sample FP6D obtained during the same sessions were less reproducible ($\mathrm{516.2}\pm \mathrm{21.2}$, $\mathrm{531.9}\pm \mathrm{14.1}$ and $\mathrm{563.4}\pm \mathrm{15.2}$ Ma), with reverse discordance in sessions two and three (Fig. 6b, c). However, ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates of these sessions are consistent ($\mathrm{500.8}\pm \mathrm{18.0}$, $\mathrm{502.5}\pm \mathrm{8.6}$ and $\mathrm{484.1}\pm \mathrm{13.5}$ Ma), yielding a total weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date of $\mathrm{497.0}\pm \mathrm{6.8}$ Ma (MSWD $=$ 0.75; $n=\mathrm{77}$). Common-Pb contents tend to be lower than in FP7G and FP12A but are often still significant. Zircon rims on baddeleyite and baddeleyite-free zircon from all SEIC samples yielded a wide range of ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates from 142 to 517 Ma (Fig. 6d, f). At least for sample FP6D, ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates become younger with increasing U contents. Zircon analyses from SEIC samples have mostly high common-Pb contents ($<$ 90 % radiogenic ${}^{\mathrm{206}}\mathrm{Pb}$). Zircon inclusions in baddeleyite (FP12A) yielded ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ date ranges of 470–733 Ma and 297–607 Ma for baddeleyite- and zircon-based RSC, respectively.

For CSMS, baddeleyite of sample S2E (Fig. 7; Tables 2 and S5) yielded weighted mean dates of $\mathrm{446.6}\pm \mathrm{15.4}$ Ma (${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$; MSWD $=$ 1.44; $n=\mathrm{21}$) and $\mathrm{436.5}\pm \mathrm{21.2}$ Ma (${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$; MSWD $=$ 0.82) from the in situ session. In contrast, the grain mount session of the same sample yielded $\mathrm{491.0}\pm \mathrm{19.8}$ Ma (${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$; MSWD $=$ 0.45; $n=\mathrm{39}$) and $\mathrm{425.5}\pm \mathrm{8.7}$ Ma (${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$; MSWD $=$ 1.00), showing reverse discordance (Fig. 7b). ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ zircon dates from grain mounts are in the range of 411–443 Ma with moderate or low common-Pb contents, but in situ dates of anhedral zircon in chlorite pseudomorphs are much younger, combined with high U and common-Pb contents. Zircon dates from S2C (Fig. S9; Table S4) are often younger than S2E baddeleyite, but most analyses show high common Pb.

For SL18, weighted mean dates are $\mathrm{202.5}\pm \mathrm{2.2}$ Ma (${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$) and $\mathrm{182.7}\pm \mathrm{12.5}$ Ma (${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$) for the grain mount session and $\mathrm{201.3}\pm \mathrm{7.2}$ Ma (${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$) and $\mathrm{177.4}\pm \mathrm{65.4}$ Ma (${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$) for the in situ session (Fig. 9; Tables 2, S6). The ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates from these sessions are in good agreement with the CAMP age of $\sim$ 201.5 Ma based on worldwide samples using zircon (Blackburn et al., 2013; Davies et al., 2017).

Figure 8

ID-TIMS U–Pb results for samples FP6D and S2E. ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates are less scattered than ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates but show a linear correlation with the percentage of discordance. All error bars and ellipses represent 2$\mathit{\sigma }$ uncertainties.

[Figure omitted. See PDF]

5.2 ID-TIMS data

ID-TIMS analyses of baddeleyite from SEIC (sample FP6D) and CSMS (sample S2E) yielded normally discordant data that form linear arrays (Fig. 8; Table 3). The upper intercept dates are $\mathrm{498.7}\pm \mathrm{4.5}$ Ma (FP6D) and $\mathrm{437.0}\pm \mathrm{7.9}$ Ma (S2E). The weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date of S2E is $\mathrm{444.1}\pm \mathrm{4.4}$ Ma (95 % confidence; MSWD $=$ 0.82), within error of the upper intercept date. In contrast, ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates of FP6D show scatter beyond uncertainty (Fig. 8c) with a weighted mean that is statistically meaningless (MSWD $=$ 5.5). For both samples, there is a direct correlation between the ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates and the percentage of discordance, leading to negative lower intercepts for linear regressions on concordia plots (Fig. 8). Like the corresponding SIMS analyses, baddeleyite analyses from FP6D and S2E contained significant common Pb (up to 6 pg). However, we tested different common-Pb isotopic compositions and blank/non-blank proportions and no geologically realistic choice produces consistent ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates for sample FP6D (see Sect. S5 for details), thus the increase in ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates with increasing discordance must be attributed to the radiogenic Pb in FP6D baddeleyite. Furthermore, the negative lower intercepts are controlled by the most discordant analyses, as a regression of the four most discordant analyses from FP6D, the ones with the most total Pb loss, leads to a lower intercept of $-\mathrm{462}\pm \mathrm{430}$ Ma (Sect. S5), negative outside of error and similar to the regression using all six analyses.

Figure 9

U–Pb baddeleyite data of sample SL18. For the SIMS analyses (a, b), error ellipses of individual analyses are $\mathrm{1}\mathit{\sigma }$, whereas the weighted mean ellipse (blue) is enlarged to $\mathrm{2}\mathit{\sigma }$. For the ID-TIMS data (c) of large crystals (blue; Data from Callegaro et al., 2017) and small crystals (red; this study), all ellipses represent $\mathrm{2}\mathit{\sigma }$ uncertainties.

[Figure omitted. See PDF]

Additional ID-TIMS data for very small baddeleyite crystals of sample SL18 (Fig. 9c; Table 3) yielded ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates that are younger than those of the larger crystals of SL18 published in Callegaro et al. (2017). All analyses overlap with Concordia within uncertainty and have low common-Pb contents ($\sim$ 0.5 pg) which are attributed to laboratory blank rather than initial common Pb or common Pb that has been added during a secondary alteration process.

Table 3

U–Pb ID-TIMS results of baddeleyite. (a) Data produced at the University of Wyoming. Sample Pb: sample Pb (radiogenic $+$ initial) corrected for laboratory blank (0.8 pg). Pbc: total common Pb. Pb${}^{*}$ $/$ Pbc: radiogenic Pb to total common Pb (blank $+$ initial). Initial Pb isotopic compositions estimated from Stacey and Kramers (1975) model. (b) Data produced at the University of Geneva.

(a)								Corrected atomic ratios								Dates (Ma)
	Weight	U	Sample Pb		Pbc	Pb${}^{*}$ $/$	Th $/$	${}^{\mathrm{206}}\mathrm{Pb}$ $/$	${}^{\mathrm{208}}\mathrm{Pb}$ $/$	${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$		${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{235}}\mathrm{U}$		${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$		${}^{\mathrm{206}}\mathrm{Pb}$ $/$	${}^{\mathrm{207}}\mathrm{Pb}$ $/$	${}^{\mathrm{207}}\mathrm{Pb}$ $/$	$\pm \mathrm{2}\mathit{\sigma }$	Rho	Discord.
Sample	($\mathrm{\mu }$g)	(ppm)	(ppm)	(pg)	(pg)	Pbc	U	${}^{\mathrm{204}}\mathrm{Pb}$	${}^{\mathrm{206}}\mathrm{Pb}$	(rad.)	% err	(rad.)	% err	(rad.)	% err	${}^{\mathrm{238}}\mathrm{U}$	${}^{\mathrm{235}}\mathrm{U}$	${}^{\mathrm{206}}\mathrm{Pb}$	abs		(%)
FP6D, Spread Eagle Intrusive complex (monzonite) – upper intercept date $\mathrm{498.7}\pm \mathrm{4.5}$ Ma (MSWD 1.7, prob. of fit 0.15) weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date $=$ $\mathrm{514}\pm \mathrm{11}$ Ma (95 % conf.; MSWD 5.5, $n=\mathrm{6}$)
#11	1.03	1000	76.1	78.4	4.4	16.8	0.06	1155	0.02	0.07844	(0.17)	0.6200	(0.33)	0.0573	(0.27)	486.8	489.8	503.9	6.0	0.57	3.52
#15	1.13	165	13.5	15.2	1.5	9.5	0.23	630	0.08	0.08005	(0.33)	0.6367	(0.88)	0.0577	(0.77)	496.4	500.3	518.1	17.0	0.48	4.34
#3	1.44	414	33.9	48.9	5.7	7.8	0.15	528	0.05	0.07754	(0.19)	0.6156	(0.47)	0.0576	(0.41)	481.4	487.1	513.6	9.1	0.49	6.50
#19	0.29	1456	105.5	30.4	1.0	28.8	0.13	1936	0.04	0.07585	(0.12)	0.6033	(0.35)	0.0577	(0.32)	471.3	479.3	517.9	6.9	0.45	9.34
#1	0.52	662	50.2	26.3	2.3	10.5	0.16	704	0.06	0.07408	(0.18)	0.5932	(0.56)	0.0581	(0.50)	460.7	472.9	532.8	11.0	0.45	14.03
#18	0.48	350	26.8	12.8	2.0	5.8	0.13	400	0.05	0.07294	(0.14)	0.5834	(0.86)	0.0580	(0.81)	453.8	466.6	530.0	17.7	0.45	14.88
S2E, Cape St. Mary's sills (granophyre) – upper intercept date $\mathrm{437.0}\pm \mathrm{7.9}$ Ma (MSWD 0.5, prob. of fit 0.68) weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date $=$ $\mathrm{444.1}\pm \mathrm{4.4}$ Ma (95 % conf.; MSWD 0.82, $n=\mathrm{5}$)
#14	0.47	370	25.2	11.8	1.6	7.0	0.03	501	0.01	0.06938	(0.19)	0.5299	(1.01)	0.0554	(0.95)	432.4	431.7	428.0	21.1	0.43	$-\mathrm{1.06}$
#18	1.02	555	37.8	38.6	3.5	10.2	0.04	713	0.01	0.06900	(0.23)	0.5303	(0.46)	0.0557	(0.38)	430.1	432.0	442.0	8.4	0.57	2.78
#33	1.31	483	30.6	39.9	1.9	20.3	0.04	1409	0.01	0.06689	(0.11)	0.5150	(0.30)	0.0558	(0.27)	417.4	421.8	446.0	6.0	0.46	6.62
#28	0.64	561	38.8	25.0	3.5	6.4	0.09	445	0.03	0.06603	(0.33)	0.5080	(1.00)	0.0558	(0.90)	412.2	417.1	444.3	19.9	0.47	7.47
#24	0.54	209	12.9	7.0	0.9	8.1	0.05	573	0.02	0.06604	(0.15)	0.5097	(1.27)	0.0560	(1.19)	412.2	418.2	451.5	26.5	0.53	8.98
(b)						Corrected atomic ratios							Dates (Ma)
	Mass U	Sample Pb	Pbc	Pb${}^{*}$ $/$	Th $/$	${}^{\mathrm{206}}\mathrm{Pb}$ $/$	${}^{\mathrm{206}}\mathrm{Pb}$ $/$		${}^{\mathrm{207}}\mathrm{Pb}$ $/$		${}^{\mathrm{207}}\mathrm{Pb}$ $/$		${}^{\mathrm{206}}\mathrm{Pb}$ $/$	$\pm \mathrm{2}\mathit{\sigma }$	${}^{\mathrm{207}}\mathrm{Pb}$ $/$	$\pm \mathrm{2}\mathit{\sigma }$	${}^{\mathrm{207}}\mathrm{Pb}$ $/$	$\pm \mathrm{2}\mathit{\sigma }$	Rho	Discord.
Fraction	(ng)	(pg)	(pg)	Pbc	U	${}^{\mathrm{204}}\mathrm{Pb}$${}^{\text{b}}$	${}^{\mathrm{238}}\mathrm{U}$${}^{\text{c}}$	$\pm \mathrm{2}\mathit{\sigma }$ %	235U c	$\pm \mathrm{2}\mathit{\sigma }$ %	${}^{\mathrm{206}}\mathrm{Pb}$${}^{\text{c}}$	$\pm \mathrm{2}\mathit{\sigma }$ %	${}^{\mathrm{238}}\mathrm{U}$	abs	${}^{\mathrm{235}}\mathrm{U}$	abs	${}^{\mathrm{206}}\mathrm{Pb}$	abs		(%)
SL18, Freetown Layered Complex – Weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date $=$ $\mathrm{201.07}\pm \mathrm{0.64}$ Ma ($\mathrm{2}\mathit{\sigma }$; MSWD $=$ 2.5, $n=\mathrm{13}$)
b1${}^{*}$	1.40	39.6	0.39	102	0.02	7073	0.031266	0.051	0.21607	0.18	0.050142	0.13	198.574	0.099	198.63	0.32	200.6	3.1	0.88	1.04
b2${}^{*}$	3.64	103	0.15	677	0.01	46 820	0.031304	0.033	0.21637	0.074	0.050153	0.048	198.810	0.064	198.89	0.13	201.0	1.3	0.66	1.16
b3${}^{*}$	2.80	79.4	0.38	211	0.01	14 578	0.031250	0.075	0.21594	0.21	0.050139	0.16	198.47	0.15	198.52	0.38	200.4	3.7	0.75	1.02
b4${}^{*}$	4.70	133	0.16	827	0.01	57 181	0.031311	0.051	0.21665	0.085	0.050206	0.056	198.856	0.099	199.12	0.15	203.5	1.5	0.65	2.34
b7${}^{*}$	2.42	68.4	0.17	393	0.01	27 202	0.031287	0.120	0.21592	0.28	0.05007	0.24	198.70	0.24	198.51	0.51	197.4	5.5	0.53	$-\mathrm{0.60}$
b9${}^{*}$	4.17	118	0.14	842	0.01	58 235	0.031280	0.081	0.21649	0.10	0.050219	0.044	198.66	0.16	198.98	0.19	204.1	1.3	0.86	2.73
b11${}^{*}$	0.75	21.3	0.28	76	0.01	5281	0.031268	0.130	0.21515	0.39	0.04993	0.33	198.59	0.26	197.87	0.69	190.6	7.7	0.55	$-\mathrm{4.15}$
b12${}^{*}$	3.97	113	0.13	870	0.01	60 188	0.031393	0.180	0.21708	0.19	0.050175	0.044	199.37	0.36	199.48	0.35	202.1	1.3	0.96	1.39
sm_b1	0.32	9.11	0.55	16	0.01	1158	0.031054	0.110	0.2136	0.79	0.04992	0.69	197.25	0.22	196.6	1.4	190	16	0.91	$-\mathrm{3.68}$
sm_b2	0.30	8.44	0.38	22	0.01	1575	0.031173	0.074	0.2145	0.50	0.04994	0.45	197.99	0.14	197.36	0.90	191	10	0.75	$-\mathrm{3.58}$
sm_b3	0.14	3.82	0.35	11	0.02	772	0.031128	0.088	0.2161	0.86	0.05036	0.80	197.71	0.17	198.6	1.6	211	19	0.69	6.26
sm_b4	0.14	3.99	0.49	8	0.02	586	0.031234	0.100	0.2165	1.1	0.05030	1.0	198.37	0.20	199.0	2.0	208	24	0.69	4.64
sm_b4-2	0.14	3.99	0.49	8	0.02	586	0.031336	0.110	0.2172	1.1	0.05030	1.0	199.01	0.21	199.6	2.0	208	24	0.68	4.34

${}^{*}$ previously reported in Callegaro et al. (2017). ${}^{\text{a}}$ Corrected for initial Th/U disequilibrium using radiogenic ${}^{\mathrm{208}}\mathrm{Pb}$ and a Th $/$ U[magma] of 2.2; ${}^{\text{b}}$ Measured ratio corrected for fractionation and spike contribution only. ${}^{\text{c}}$ Measured ratios corrected for fractionation, tracer, blank and, where applicable, initial common Pb.

6 Discussion

6.1 Occurrence, textures and interrelations of accessory minerals

Zirconium-bearing accessory minerals in mafic magmas form during late stages of crystallization in more differentiated interstitial melt (Heaman and LeCheminant, 1993; Schaltegger and Davies, 2017). In our study, abundance and crystal size of accessory minerals lack a strong correlation with whole-rock Zr content (Sect. S7), but the more coarse-grained samples tend to contain larger baddeleyite and zircon crystals. Regardless of crystal sizes, baddeleyite and zircon in SEIC and CSMS rocks form various types of intergrowths. Baddeleyite in mafic rocks is typically of igneous origin, but metamorphic processes can cause it to react to polycrystalline zircon (Heaman and LeCheminant, 1993). Metamorphic zircon is therefore expected to be the most common type of zircon intergrown with baddeleyite in SEIC and CSMS rocks, which all have experienced low-grade metamorphism. Although probably less common, magmatic zircon overgrowths on pre-existing baddeleyite can also form during late-stage igneous crystallization due to an increased ${\mathrm{SiO}}_{\mathrm{2}}$ activity in the melt (e.g., Renna et al., 2011). Such igneous zircon overgrowths on baddeleyite have rather euhedral crystal faces and straight interfaces with baddeleyite (Renna et al., 2011). By contrast, metamorphic zircon shares more irregular crystal interfaces with baddeleyite and has an anhedral exterior, described as “raspberry texture” (Heaman and LeCheminant, 1993) or “frosty appearance” (Söderlund et al., 2013). For SEIC and CSMS, the typical textural features of igneous zircon overgrowth on baddeleyite are rarely displayed (Fig. 5l), whereas features of metamorphic replacement zircon are frequently observed. Zircon seems to pseudomorphically replace baddeleyite, accompanied by feather-like zircon coronas (e.g., Figs. 4d, 5l), probably due to volume enlargement by the addition of silica during metamorphism. The presence of such coronas can therefore help to distinguish zircon with a baddeleyite precursor from primary zircon in altered igneous rocks.

The extent of baddeleyite replacement by zircon in this study often depends on the host minerals. Baddeleyite surrounded by chlorite shows replacement by zircon more commonly than baddeleyite in albite or epidote group minerals, and baddeleyite inclusions in K-feldspar mostly lack zircon. We attribute this to local variations in the ${\mathrm{SiO}}_{\mathrm{2}}$ activity during metamorphism: the chloritization of pyroxenes liberates large amounts of Si, whereas alteration of alkali feldspars has a neutral Si balance. Si release sometimes also causes replacement of zirconolite by titanite $+$ zircon (Fig. 3g) or titanite $+$ gittinsite (Fig. 5o).

Alteration by fluids with high ${\mathrm{SiO}}_{\mathrm{2}}$ activity causes baddeleyite replacement by zircon, but fluids poor in Si and rich in Ca can induce the opposite effect even in siliceous rocks (Lewerentz et al., 2019). In sample S2C, multiple micrometer-sized baddeleyite inclusions are hosted in the outer zones of zircon, which shows porous domains (Fig. 5a), cracks (Fig. 5c), and high contents of common Pb, which are typical alteration features (e.g., Corfu et al., 2003; Rayner et al., 2005; Aranovich et al., 2017). Whereas other fluid-mediated processes may also be capable of forming secondary baddeleyite inclusions in altered zircon (Lewerentz et al., 2019), the former presence of fluids with high Ca $/$ Si ratio in S2C is likely due to widespread albitization of plagioclase. Previously reported occurrences of secondary baddeleyite inclusions in zircon are from rocks that experienced high-temperature (mostly amphibolite facies) alteration (Barth et al., 2002; Aranovich et al., 2013, 2017; Lewerentz et al., 2019), and experiments reproducing this texture were conducted at 600 and 900 ${}^{\circ }$C (Lewerentz et al., 2019). However, Cape St. Mary's sills have experienced only subgreenschist facies (Greenough and Papezik, 1986b) or, at most, lower greenschist facies conditions. Hence, we present the first evidence that secondary baddeleyite inclusions in zircon can also form at low temperatures, and low-temperature reactions of zircon to baddeleyite and vice versa can occur within the same dike.

A peculiar texture in sample FP12A is baddeleyite with zircon inclusions (Fig. 4e–k). BSE and CL images provide only two-dimensional petrographic information, so it can be argued whether these are only apparent inclusions as part of metamorphic zircon rims that locally penetrate the crystal. However, most of these baddeleyite crystals lack any visible zircon overgrowth, and the baddeleyite mantle is coherent even when as thin as 1 $\mathrm{\mu }$m. Furthermore, we observed this texture repeatedly in sample FP12A but not in other samples. Thus this texture most likely represents actual zircon inclusions of xenocrystic origin. An attempt to test this hypothesis with SIMS dating of these zircon inclusions yielded an older ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ date only for one crystal (Fig. 4e; Table S3, analysis 1_3) but the primary beam overlapped both the baddeleyite and zircon. Furthermore, difficulties with the RSC (see Sect. 6.2.1) and/or Pb loss from possibly metamict zircon may have biased the results. Lastly, the xenocrysts may be derived from an assimilated Cambrian or Ediacaran sedimentary country rocks, whose detrital zircon is often not much older than ca. 500 Ma (Pollock et al., 2009), which is roughly the age of FP12A.

In a hot, low ${\mathrm{SiO}}_{\mathrm{2}}$ activity magma such as the primary magma of FP12A, xenocrystic zircon is undersaturated and dissolves (see Boehnke et al., 2013). Slow Zr diffusion in the melt limits the zircon dissolution rate, so that the melt adjacent to the zircon will develop an exponentially decreasing Zr concentration gradient (e.g., Harrison and Watson, 1983). Hence, partially dissolved xenocrystic zircon will be surrounded by a halo of elevated Zr concentration in the zircon-undersaturated magma. Such a halo of elevated Zr concentrations is a preferential location for baddeleyite nucleation, even if the bulk of the magma remains undersaturated with regard to baddeleyite. Once a nucleus is formed, baddeleyite will grow preferentially where Zr concentration is highest (at the dissolution interface). If a coherent baddeleyite mantle is formed, the zircon xenocryst becomes shielded from further dissolution.

Although such xenocrystic inclusions can be overlooked easily, the lack of previous reports suggests that this is a rare texture. This may be a consequence of numerous factors:

• A melt with low ${\mathrm{SiO}}_{\mathrm{2}}$ activity is needed, being zircon-undersaturated, but close to baddeleyite saturation.

• The country rock must have zircon but should not be too siliceous, because otherwise zircon would be stabilized and baddeleyite destabilized. If the country rock is only weakly consolidated, zircon liberation is facilitated.

• High temperatures and low crystal fraction of the magma are necessary to assimilate country rock effectively. However, this also favors rapid dissolution of zircon or xenocrysts or their entrapment in major phases before baddeleyite saturation is achieved.

• In specific cases, baddeleyite may fail to enclose zircon before the latter dissolves completely. This may leave a notch on the baddeleyite crystal, such as in Fig. 4e and k.

Table 4

Compilation of all known baddeleyite (Bad)–zircon (Zrn) intergrowth types and guideline for their interpretation.

Appearance in		Common	Age
BSE image	Type	textural features	relationship	Rock types	References
	Igneous Bad replaced by metamorphic Zrn	Frosty or raspberry-like Zrn rims or feather-like Zrn coronas; pseudomorphism; irregularcrystal interfaces	Bad $>$ Zrn	High- and low-grade meta-igneous rocks	Heaman andLeCheminant (1993); Söderlundet al. (2013); thisstudy
	Late igneousZrn rim onigneous Bad	Euhedral Zrn rims;straight interfaces withBad	Bad $>$ Zrn ($\approx$)	Igneous rockswhich recordthe overstep of ${\mathrm{SiO}}_{\mathrm{2}}$ oversaturation	Renna et al.(2011)
	Igneous Badwith xenocrystic Zrn inclusions (?)	Complete Bad mantlearound Zrn	Bad $<$ Zrn	Gabbros; probably other igneous rocks	This study
	Bad with Zrnrim closed toimpact meltpockets	Bad often deformed,with degraded crystallinity or disintegrated into granular droplets;Zrn rims discontinuous up to a few $\mathrm{\mu }$m	Bad $>$ Zrn	Meteorites	Moser et al. (2013); Darling et al.(2016)
	Zrn decomposition during impact melting	Droplets of Bad orother ${\mathrm{ZrO}}_{\mathrm{2}}$ polymorphs; Zrn often with deformation featuressimilar to Bad in (d)	Bad $<$ Zrn	Impact glasses	El Goresy(1965); Wittmannet al. (2006)
	Desilification Bad on mantle-derived Zrn	Feather-like Bad rim(often intergrown withdiopside) on a Zrnmegacryst	Bad $<$ Zrn ($\approx$)	Kimberlites	Kresten(1973); Heamanand LeCheminant (1993)
	Altered igneous Zrn with secondary Bad inclusions	Bad often arrangedalong the Zrn zonationor along cracks	Bad $<$ Zrn	Altered igneous rocks, including siliceousrocks	Lewerentz etal. (2019); thisstudy

Our detailed micropetrography revealed that baddeleyite and zircon can be intergrown in various ways, especially for samples with complex metamorphic histories. Including our newly proposed xenocrystic zircon inclusions in baddeleyite, at least seven different types of baddeleyite–zircon intergrowths have to be considered (compiled in Table 4). Three of these types are not observed in our samples: (1) granular baddeleyite droplets can rim zircon that decomposed to baddeleyite $+$ ${\mathrm{SiO}}_{\mathrm{2}}$ as a result of impact shockwave heating (e.g., El Goresy, 1965; Wittmann et al., 2006). (2) The inversion of this reaction was found in a shergottite sample, where primary baddeleyite is often partially rimmed by polycrystalline zircon in the vicinity of impact melt (Moser et al., 2013; Darling et al., 2016). This is the only baddeleyite–zircon intergrowth type where baddeleyite is affected by shockwave metamorphism (Moser et al., 2013; Darling et al., 2016). (3) Feather-like polycrystalline baddeleyite reaction rims on mantle-derived zircons in kimberlites were found to be the result of desilicification reactions (Kresten, 1973). These seven intergrowth types can occur in combination, complicating textural interpretation. Dating by SIMS or LA-ICP-MS provides the high spatial resolution that is required to unravel the age relationships of baddeleyite–zircon intergrowths. Alternatively, dissolution in hydrochloric acid alone may avoid including zircon domains in ID-TIMS baddeleyite analyses (e.g., Rioux et al., 2010).

6.2 Interpreting intrusion ages from nonideal baddeleyite

6.2.1 Challenges in baddeleyite geochronology by SIMS

Despite many examples of good agreement between SIMS and ID-TIMS data (e.g., the SIMS ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date agrees with the ID-TIMS ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ and upper intercept dates of FP6D, the SIMS in situ dates agree with both ID-TIMS dates of S2E, and all dates of SL18 and FC-4b agree), some SIMS sessions yielded significantly deviating dates, notably in the case of grain mount sessions and/or ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates. Although SIMS dates of baddeleyite can be more accurate than ID-TIMS dates in certain cases (see Sect. 6.2.3 and 6.2.4), baddeleyite poses analytical challenges that are specific for in situ methods: beam overlap on adjacent phases and possible bias in the U $/$ Pb relative sensitivity calibration (RSC).

Small crystal sizes of baddeleyite ($<$ 10 $\mathrm{\mu }$m) often result in primary beam overlap on adjacent phases during SIMS sessions. This does not necessarily affect the accuracy of baddeleyite dates if the adjacent minerals are U and Pb free (e.g., chlorite), but otherwise, especially in the case of intergrowths with zircon and zirconolite, accuracy of baddeleyite dates can be severely affected. But even so, estimations of the baddeleyite crystallization ages are possible if the extents of potential resulting inaccuracies can be assessed. This requires knowledge about (1) the approximate U–Pb crystallization ages of baddeleyite and the contaminating phase – we suppose that the zircon rims of SEIC samples formed at ca. 400 Ma during the Acadian Orogeny, being ca. 20 % younger than SEIC baddeleyite, and that some of the zircon rims experienced Pb loss; (2) possible differences in U content of the involved minerals – baddeleyite tends to have the same (this study) or higher (Heaman and LeCheminant, 1993) U contents than zircon and lower U contents than zirconolite (Rasmussen and Fletcher, 2004); and (3) matrix effects that lead to different U $/$ Pb relative sensitivities. As observed from the RSC, baddeleyite ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates shift to younger ages when computed against a zircon RSC ($-\mathrm{54}$ to $+$3 % total, $-\mathrm{23}$ % average), and zircon dates become older vice versa ($+$1 % to $+$121 %, $+$43 % average). Similar bias results from baddeleyite–zirconolite beam overlap, although presently this bias cannot be quantified due to lack of well-characterized zirconolite reference materials. Notably, when SIMS baddeleyite analyses contain metamorphic zircon contributions, their younger age is partly compensated by the RSC bias, so their influence on data quality is less severe than in the cases where zircon is coeval or older than baddeleyite.

Precision and accuracy of SIMS ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates strongly depend on the quality of the RSC. Variable degrees of reverse discordance in different SIMS grain mount sessions of the same sample most likely reflect difficulties in quantification of matrix effects. RSC accuracy depends on numerous factors, but crystal orientation effects have been long recognized as particularly important for SIMS U–Pb dating of baddeleyite (Wingate and Compston, 2000). Although oxygen flooding of the sample chamber proved to be effective for reducing crystal orientation effects, residual bias remains (Schmitt et al., 2010; Li et al., 2010). In the case of grain mounts, tabular crystals will be preferentially oriented with their c axis parallel to the sample surface. This may be a cause of matrix mismatch in grain mount analyses, whereas in situ mounts, which lack reverse discordance in this study, are expected to have more random distributions of crystal orientations. Analysis of a sufficiently large number of crystals ($>$ ca. 25) and randomizing crystal orientations of grain mounts may lead to more accurate SIMS ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ baddeleyite dates. However, crystal orientation effects, if present, would also be expected for the secondary reference baddeleyite FC-4b, which nevertheless yielded ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates in agreement with published ID-TIMS data (Schmitt et al., 2010), although it was analyzed during the same grain mount sessions as FP6D and S2E baddeleyite. Hence, other factors such as alteration may be more significant for the RSC than crystal orientation.

6.2.2 Common Pb in Zr-bearing minerals

Ideal U–Pb mineral geochronometers exclude common Pb during crystallization, a behavior that baddeleyite, zircon and zirconolite approximately fulfill (e.g., Heaman and LeCheminant, 1993; Rasmussen and Fletcher, 2004). However, in our samples, all three minerals often contain abundant common Pb, as evident from SIMS and ID-TIMS analyses of SEIC and CSMS (Tables 3 and S1–S6). Similar abundances of common Pb were also detected in baddeleyite from other mafic dikes (e.g., Olsson et al., 2011). Adjacent phases, surface contamination (SIMS), laboratory blank (ID-TIMS) and mineral inclusions (SIMS and ID-TIMS) can be external sources of common Pb, but steady ${}^{\mathrm{204}}\mathrm{Pb}$ counting rates even in some SIMS analyses with the spot entirely on baddeleyite demonstrate that some amount of common Pb is intrinsic to these crystals. In the case of zircon, it is known that common Pb can be incorporated during alteration (e.g., Watson et al., 1997; Rayner et al., 2005; Geisler et al., 2007). By analogy, the interplay of radiation damage and interaction with fluids may trigger a similar process in baddeleyite and zirconolite. Alteration could also modify the chemical composition of baddeleyite and may therefore bias the RSC, but a correlation of ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ date and common-Pb content is detectable only for sample FP7G, which also shows a correlation of common-Pb content and the (RSC-independent) ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date. Moreover, common-Pb contents of baddeleyite in FP7G and FP12A increase with decreasing U content, making it difficult to explain common-Pb incorporation with radiation damage, unless U was mobilized as well. Uranium mobilization can cause normal or reverse discordance and may therefore be detectable by further ID-TIMS analyses. Furthermore, baddeleyite and zircon can be expected to alter differently, as baddeleyite is more resistant to radiation damage (Schaltegger and Davies, 2017). Oxygen isotope analysis by SIMS has been suggested as a tool to detect baddeleyite alteration (Davies et al., 2018), although its routine use is still in its infancy. Zirconolite, which only allows for ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dating (Rasmussen and Fletcher, 2004), shows high common-Pb abundances in sample FP7G (45 %–93 % radiogenic ${}^{\mathrm{206}}\mathrm{Pb}$), being therefore unsuited as a geochronometer for altered samples.

6.2.3 Baddeleyite discordance

Although volume diffusion of Pb in baddeleyite is thought to be extremely slow (Heaman and LeCheminant, 2000), baddeleyite analyses often show a few percent of discordance. Naturally observed discordance patterns range from linear and complex arrays to uniform clusters beneath concordia (e.g., Söderlund et al., 2013; Schaltegger and Davies, 2017; Heaman and LeCheminant, 2000; Ibañez-Mejia and Tissot, 2019). This underscores that discordance is not always created by the same mechanism, and it is crucial for age interpretation to identify the correct discordance mechanism(s) in the specific sample by means of the discordance pattern (Fig. 10). If contributions from metamorphic zircon rims have caused discordance, a three-component mixing model can be applied, with end-members defined by (1) the igneous crystallization age of baddeleyite, (2) metamorphic formation of zircon, and (3) recent Pb loss of zircon and/or baddeleyite (Söderlund et al., 2013). The oldest ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date would then yield a minimum estimate of 1. In contrast, ${}^{\mathrm{231}}\mathrm{Pa}$ excess would influence only the ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{235}}\mathrm{U}$ decay system, making ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ ages most accurate (Amelin and Zaitsev, 2002; Crowley and Schmitz, 2009) and vice versa in the case of ${}^{\mathrm{222}}\mathrm{Rn}$ loss (Heaman and LeCheminant, 2000). Pb loss due to alpha recoil or fast pathway diffusion (e.g., along twin planes) affects both systems similarly, making ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ ages most accurate (Davis and Davis, 2018).

Figure 10

Schematic model of the consequences of different discordance mechanisms on the isotopic composition of baddeleyite.

[Figure omitted. See PDF]

Metamorphic zircon overgrowth was absent in baddeleyite used for ID-TIMS analysis of S2E and SL18. Even in FP6D, where it is petrographically evident, the ID-TIMS data appear to be free of a significant isotopic component of metamorphic zircon. This confirms that baddeleyite and zircon can be separated successfully with the method of Rioux et al. (2010), using only hydrochloric acid for dissolution. Consequently, discordance in our samples should be attributed rather to baddeleyite itself than to zircon intergrowths. Our ID-TIMS analyses show linear arrays that are typical for varying degrees of recent Pb loss. The portion of radiogenic Pb lost by alpha recoil can be predicted based on crystal shapes (Davis and Davis, 2018) and is generally $<$ 0.3 % for the crystals of this study. However, Pb loss indicated for our samples exceeds this extent often by more than 1 order of magnitude (Table 3). Hence alpha recoil can explain only a small part of the discordance observed for FP6D, S2E and SL18, depending on the U zonation of the crystals. Fast pathway and/or volume diffusion is therefore likely to dominate baddeleyite discordance here. The radiation dose does not seem to be crucial: except for the in situ session of S2E, negative correlations between U content and ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates appear to be absent in SIMS and ID-TIMS data of our samples (cf. Söderlund et al., 2013).

Intriguingly, the discordia trends for samples FP6D and S2E have negative lower intercepts and show a positive correlation of the ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date with the percentage of discordance (Fig. 8). Similar discordance patterns have been observed from baddeleyite ID-TIMS analyses of the Duluth gabbro (Hoaglund, 2010; Ibañez-Mejia and Tissot, 2019) which plot essentially within the concordia error swath, but yielded older ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates, younger ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates and undistinguishable ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{235}}\mathrm{U}$ dates compared to coexisting zircon. These studies interpreted ${}^{\mathrm{231}}\mathrm{Pa}$ excess to be responsible for this pattern, which cannot be excluded as evidence for modest amounts of excess ${}^{\mathrm{231}}\mathrm{Pa}$ was recently obtained from young baddeleyite (Sun et al., 2020). However, the negative lower intercepts for our Newfoundland samples would require that the magnitude of ${}^{\mathrm{231}}\mathrm{Pa}$ excess increases with discordance, which is difficult to rationalize. For the Duluth gabbro analyses, the overlap of baddeleyite and zircon ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{235}}\mathrm{U}$ dates is impossible to produce with ${}^{\mathrm{231}}\mathrm{Pa}$ excess alone. We therefore propose preferential loss of ${}^{\mathrm{206}}\mathrm{Pb}$, possibly due to ${}^{\mathrm{222}}\mathrm{Rn}$ mobility, as a more likely explanation of these peculiar patterns (see Heaman and LeCheminant, 2000), as such excess ${}^{\mathrm{206}}\mathrm{Pb}$ loss could simply increase with overall Pb loss (see Sect. S6 for more details). Negative lower intercepts have rarely been reported in previous baddeleyite dating studies, suggesting that they are either caused by a rare process or are often masked by uncertainties and/or additional discordance mechanisms.

Our data also imply that baddeleyite rims are more strongly affected by Pb loss than cores. The ID-TIMS data of SL18 (Fig. 9c) show younger ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates for the smallest crystals, which have larger surface to volume ratios than the larger crystals. Furthermore, the ID-TIMS analyses of large SL18 baddeleyite yielded younger ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates than the SIMS analyses (Table 3 vs. Table S6). The SIMS spots were typically placed in the centers of the grains, avoiding the apparently less discordant rims, whereas dissolution of the plucked grains for ID-TIMS analysis included them, resulting in more discordant ID-TIMS analyses. Admittedly, it cannot be excluded that SIMS ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ data of the relatively pristine SL18 baddeleyite may be also affected by RSC bias, similar to the altered Newfoundland samples. However, this concern is irrelevant for the ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ data, which agree within error between SIMS and ID-TIMS for SL18, but ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates from the more discordant Newfoundland samples tend to be older for ID-TIMS than for SIMS. This may imply that baddeleyite rims in FP6D have undergone preferential ${}^{\mathrm{206}}\mathrm{Pb}$ loss, which would drive the more discordant ID-TIMS analyses towards older ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates. In any case, fast pathway and/or volume diffusion can both explain intensified Pb loss from crystal rims, but to differentiate between these processes, both the U zonation within the crystals and the post-emplacement thermal history of the samples are not sufficiently known.

6.2.4 Implications for baddeleyite dating approaches

Targeting the least altered and most coarse-grained samples in the field is highly advantageous for recovery of pristine baddeleyite which often yields concordant ages. However, as the examples of SEIC and CSMS rocks show, alteration can be ubiquitous in certain geologic units, so that usage of texturally complex, discordant baddeleyite is inevitable. But even baddeleyite from unaltered samples, such as SL18, often shows evidence for minor Pb loss (see also Söderlund et al., 2015). With Pb loss as a dominant discordance mechanism, ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates of baddeleyite often underestimate intrusion ages, whereas ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates are more accurate. In the case of SIMS, another advantage of ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates is their independence from the RSC. This favors the use of ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ rather than ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ ages even for Phanerozoic baddeleyite, in spite of its typically lower precision. For Mesozoic samples such as SL18, however, comparatively low precisions of SIMS data make it difficult to use ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates meaningfully, although improved ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ precisions have been achieved with a multicollection SIMS method (Li et al., 2009). Another limitation for ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates is possible bias by preferential ${}^{\mathrm{206}}\mathrm{Pb}$ loss, as suggested by the correlation of ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates with the percentage of discordance (Fig. 8). If this bias is important, the ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates of the least discordant analyses are most accurate, and more discordant analyses should be excluded from weighted mean calculations. Alternatively, if the excess ${}^{\mathrm{206}}\mathrm{Pb}$ loss is a linear function of total Pb loss, upper intercept dates are the most accurate. This can be shown for sample FP6D, where the upper intercept date from ID-TIMS ($\mathrm{499}\pm \mathrm{5}$ Ma) and the ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date from SIMS ($\mathrm{497}\pm \mathrm{7}$ Ma) are indistinguishable but most of the ID-TIMS ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates are considerably older (504–530 Ma, Table 3, Fig. 8). If baddeleyite cores are less discordant than rims, the cores should be preferentially targeted for analysis, which is easier to achieve with SIMS. In the case of ID-TIMS, mechanical abrasion is potentially helpful in this respect, and there are documented cases where discordance was reduced by mechanical abrasion (e.g., Corfu and Lightfoot, 1996; cf. Greenough et al., 1993). Alternatively, baddeleyite cores can be cut out with a focused ion beam before ID-TIMS analysis (White et al., 2020).

6.2.5 Intrusion ages of the SEIC, CSMS and FLC

Stratigraphic constraints require that the SEIC is coeval with the Cambrian volcano-sedimentary succession on the western Avalon Peninsula (Sect. 2.1). Trilobite biostratigraphy suggests that the age span of deposition of the Manuels River Formation roughly equals that of the Drumian stage (Hildenbrand, 2016; Austermann, 2016), which is currently calibrated from 504.5 to 500.5 Ma with uncertainties on these bounds of ca. 2 Ma (Peng et al., 2012). The occurrence of pillow lavas in the Chamberlain's Brook Formation and Elliot Cove formation expands the age range of Cambrian volcanism on the Avalon Peninsula to both pre- and post-Drumian (Fig. 2). Our SIMS and ID-TIMS data are thus in good agreement with these stratigraphic constraints. We regard the ID-TIMS concordia upper intercept date of FP6D ($\mathrm{498.7}\pm \mathrm{4.5}$ Ma) as the best available estimate of the intrusion age of the corresponding feeder pipe, as it is more likely unbiased by the sample-specific baddeleyite discordance mechanisms than the ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ and ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates. As indicated by the stratigraphic distribution of volcanic rocks, the other feeder pipes may be significantly older and/or younger, but this first radiometric age for the SEIC indicates that SEIC magmatism clearly predates the opening of the Rheic Ocean (see Sect. 2).

Figure 11

Recalculated age for the Cape St. Mary's sills using only the ID-TIMS data of Greemough et al. (1993) and this study which are $<$ 3 % discordant.

[Figure omitted. See PDF]

For the CSMS, zircon from granophyre sample S2C is considerably altered and the degree of secondary Pb loss is often very large (Sect. S4), limiting its use for geochronology. Baddeleyite from sample S2E, although potentially also altered, better preserves the igneous age. Our ID-TIMS ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ baddeleyite date ($\mathrm{444.1}\pm \mathrm{4.4}$ Ma) agrees within error with that of Greenough et al. (1993), and the samples of both studies are derived from the same granophyric dike (John D. Greenough, personal communication, 2019). Greenough et al. (1993) analyzed bulk separates of baddeleyite, and the large number of crystals per aliquot in their analyses enhanced precision due to stronger Pb signals, but may have obscured the discordance patterns that we observed in our single-crystal analyses. Combining the data of both studies, we regard a weighted mean ID-TIMS ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ age of $\mathrm{439.4}\pm \mathrm{0.8}$ Ma (95 % conf.; MSWD $=$ 0.94; Fig. 11) as the best available estimate of the intrusion age of the Lance Cove sill, using only the analyses with $<$ 3 % discordance to minimize bias due to possible preferential ${}^{\mathrm{206}}\mathrm{Pb}$ loss. If this bias is significant even for the least discordant analyses, this ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date may be an overestimate, but the ID-TIMS upper intercept date of $\mathrm{437}\pm \mathrm{8}$ Ma, which would be more accurate in this case, does not lead to a better age estimate due to inferior precision. The date that we report does not rule out the possibility that other sills of Cape St. Mary's are significantly older or younger.

For the FLC, our new ID-TIMS and SIMS data suggest that the intrusive age based on a weighted mean ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ date reported in Callegaro et al. (2017) from large baddeleyite crystals is likely too young and reflects some degree of Pb loss. The small baddeleyite crystals from SL18 yielded younger ID-TIMS ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ dates due to more intense Pb loss, likely due to fast pathway or volume diffusion. Therefore, we regard the weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ ID-TIMS date ($\mathrm{201.07}\pm \mathrm{0.64}$ Ma) as the best estimate for the intrusion age of SL18. This age is in agreement with the SIMS dates and all other age constraints from both the FLC and the CAMP (Davies et al., 2017; Callegaro et al., 2017). This new age does not change the overall interpretations of Callegaro et al. (2017). The good agreement of the SIMS and ID-TIMS dates from sample SL18 validates that baddeleyite dating by SIMS, which has been applied so far mostly for Precambrian and early Paleozoic samples (e.g., Schmitt et al., 2010), can also yield accurate ages for Mesozoic samples.

7 Conclusions

Based on new and published microtextural observations, at least seven different types of baddeleyite–zircon intergrowths can be identified. Secondary baddeleyite inclusions in zircon can also form during low-temperature alteration. Furthermore, we interpret a previously undocumented texture as xenocrystic zircon cores mantled by igneous baddeleyite overgrowths.

SIMS ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ data, at least from grain mounts, show bias in the U $/$ Pb relative sensitivity calibration, possibly due to crystal orientation effects and/or alteration.

Unusually high common-Pb contents in baddeleyite are evident from SIMS and ID-TIMS data of the same crystals and probably a consequence of alteration.

For our samples, we identified secondary Pb loss, due to fast pathway and/or volume diffusion, as the dominant discordance mechanism. Correlations between ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ dates and the degree of discordance imply that there may be a component of preferential ${}^{\mathrm{206}}\mathrm{Pb}$ loss, possibly due to ${}^{\mathrm{222}}\mathrm{Rn}$ mobility. Baddeleyite rims appear to be more affected by Pb loss than cores.

Any kind of Pb loss makes ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ ages more reliable than ${}^{\mathrm{206}}\mathrm{Pb}{/}^{\mathrm{238}}\mathrm{U}$ ages, even for Phanerozoic baddeleyite. In the case of preferential ${}^{\mathrm{206}}\mathrm{Pb}$ loss, the most accurate age is either the concordia upper intercept date or the weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date of the least discordant analyses. Improved concordance of baddeleyite dates may be achieved when preferentially targeting the less discordant crystal cores, either by SIMS spot analysis, or possibly by applying mechanical abrasion prior to ID-TIMS analysis.

We present new and refined intrusion ages for the Spread Eagle Intrusive Complex, Newfoundland ($\mathrm{498.7}\pm \mathrm{4.5}$ Ma, ID-TIMS concordia upper intercept), which formed during rifting before the opening of the Rheic Ocean, as well as for Cape St. Mary's sills, Newfoundland ($\mathrm{444.1}\pm \mathrm{4.4}$ Ma, ID-TIMS weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date of the least discordant analyses), and the Freetown Layered Complex, Sierra Leone ($\mathrm{201.07}\pm \mathrm{0.64}$ Ma, ID-TIMS weighted mean ${}^{\mathrm{207}}\mathrm{Pb}{/}^{\mathrm{206}}\mathrm{Pb}$ date).

Data availability

All research data are given in Table 3 and in the supplementary tables of this article.

The supplement related to this article is available online at: https://doi.org/10.5194/gchron-2-187-2020-supplement.

Author contributions

This study is partly based on the MSc thesis of JEP, supervised by AKS. GA and AH applied for funding and helped with fieldwork. SIMS analyses were performed by JEP (SEIC, CSMS), AKS and KRC (SL18). ID-TIMS analyses were performed by KRC (SEIC, CSMS) and JHFLD (SL18). Geochronological interpretations developed from discussions between JEP, KRC and AKS with additions by JHFLD. JEP wrote the article with support from all co-authors.

Competing interests

The authors declare that they have no conflict of interest.

Acknowledgements

Ilona Fin and Oliver Wienand prepared thin sections and epoxy mounts. Robert B. Trumbull (Helmholtz Centre Potsdam – GFZ Potsdam) contributed whole-rock geochemical data (see Table S7, Figs. S10–S12).

Financial support

This project is funded by the Klaus Tschira Foundation (03.131.2017 Förderung von Abschlussarbeiten (MSc und BSc) in Verbindung mit Projekt 00.272.2015 “Kambrium von Avalonia mit Schwerpunkt Ostneufundland”). Further support came from the German Research Foundation (DFG Scientific Instrumentation and Information Technology program). Kevin R. Chamberlain was partially supported from Mega-Grant 14.Y26.31.0012 and RNF grant 18-17-00240 of the government of the Russian Federation.

Review statement

This paper was edited by Daniela Rubatto and reviewed by Ulf Söderlund and one anonymous referee.