Field mapping at the quarries and along the ridge that connects them has been ongoing since 2009. We sampled and made measurements at a variety of scales. We measured >100 individual pillow lava sizes and orientations using meter tape measures and Brunton compasses with clinometers. Trend and plunge data of pillow basalts for each locality were plotted using Stereonet (v. 11.4.5 Allmendinger et al., 2013; Cardozo and Allmendinger, 2013). Data were contoured using the Kamb contouring method. The average trend and plunge direction for pillows at each locality was calculated based on the center of the contoured pi-maxima. Data from localities close to each other were compared; if averages were similar, then the data were merged into one plot that represented a larger area.

A variety of approaches have been used to map vertical faces in the quarries, including laser range-finding, Gigapan technology, Structure-from-Motion, and drones. Sample and data collection sites were located using standard handheld GPS units, which are generally considered to have non-corrected positional errors of ± 5 m or less. For samples where accurate elevations are critical, we used the Arctic DEM subsampled to 1.8 m resolution to subsequently correct sample elevations to a consistent elevation model.

We note here that quarries, while providing unparalleled exposures and access to fresh samples, can have inherent disadvantages. For example, our field observations are largely centered on pillow lava units, which now dominate the stratigraphy at both quarries. It is possible that the unconsolidated tuff-breccia units originally occupied a larger proportion of the quarries but have been preferentially removed due to ease of mining.

Major and trace elements were measured on a total of 89 whole-rock samples, including 6 bombs from fragmental units, 57 pillow lavas, and 26 intrusions (Table 1; Supplementary Table SA1). Whole-rock powders from fresh samples were prepared in alumina grinding containers and sieved through 325 mesh. Loss on ignition (LOI) was determined by heating the powders for 1 h at 950°C following Boyd and Mertzman (1987). Most samples were analyzed for major elements by X-ray fluorescence spectroscopy (XRF; 86 samples) at the College of Wooster following the methods of Pollock et al. (2014). The XRF was drift corrected prior to each run and repeat analyses of standards shows reproducibility <2%. Most trace elements were measured by inductively coupled plasma mass spectrometry (ICP-MS; 71 samples) at the Peter Hooper Lab, Washington State University, United States following standard methods (Lichte et al., 1987; Jarvis, 1988; Doherty, 1989; Jenner et al., 1990; Longerich et al., 1990). Analytical runs consisted of unknowns, standards, and drift correction solutions. Reproducibility is <5% for rare Earth elements and <10% for all other elements. Full analytical precision and accuracy details for XRF and ICP-MS analyses are provided in the Supplementary Tables SA2–SA4). A few samples (3) were analyzed at Duke University by directly coupled plasma atomic emission spectroscopy (DCP-AES) and ICP-MS following the methods of Klein et al. (1991); Cheatham et al. (1993), respectively. DCP-AES analyses show reproducibility of 1%–2% for all major elements with the exception of K₂O (∼10%) and P₂O₅ (< 8%). ICP-MS analyses at Duke show reproducibility of 1%–5% for trace elements. Full quality assurance data for the Duke analyses are provided in the Supplementary Material to Pollock et al. (2014). Interlab comparison of duplicate samples analyzed by ICP-MS at Duke and Washington State Universities shows good agreement between methods (Supplementary Table SA5).

Sr-Nd-Pb isotope ratios were measured on seven whole-rock powders from Undirhlíðar and Vatnsskarð quarries by thermal ionization mass spectrometry (TIMS) at the University of North Carolina at Chapel Hill (Table 2). Samples were dissolved and cations were separated following the methods of (Miller and Glazner, 1995). Measurements were made on a VG Sector 54 mass spectrometer. Sr isotopes are referenced to ⁸⁷Sr/⁸⁶Sr = 0.710231 ± 9 (NBS 987, n = 9). Nd isotopes are referenced to ¹⁴⁶Nd/¹⁴⁴Nd = 0.512102 ± 10 (JNdi, n = 20).

Volatiles (H₂O and CO₂) were measured on pristine glassy rims from 38 pillow lavas. In Undirhlíðar quarry, seven samples were collected from a cluster of adjacent pillows, four of which were collected from a single pillow (Table 3). For most samples, three glass chips were selected for analysis. Glass chips ranged in size from <1 mm to 7 mm in diameter and were chosen to avoid significant weathering, alteration, phenocrysts, and vesicles. Chips were doubly polished into 100–200 micron-thick wafers. Thickness of each glass wafer was measured three times and averaged for each chip for a precision of ± 5 microns. Wafers were analyzed by Fourier Transform Infrared Spectroscopy (FTIR) at the University of Massachusetts Amherst on a Bruker Tensor 27 FTIR with attached Hyperion 3000 microscope. FTIR spectra were obtained for a 10 × 10 micron area using OPUS (version 7.2) software. Care was taken to avoid measuring sites adjacent to fractures, vesicles, crystals, and margins. At least three sites were measured for each chip, so each value reported represents the average of 3–12 spectra. Individual FTIR measurements are presented in the (Supplementary Table SA7).

IR peak absorbance at ∼3529 cm^-1 was used to calculate total water (H₂O_t) concentration using the Beer-Lambert Law (Stolper, 1982). Glass density was 2,750 ± 55 g/L, estimated using Bottinga and Weill (1972) and based on average composition of the sample suite. The molar absorption coefficient for H₂O in basalt was 63 ± 3 L/mol-cm (Dixon et al., 1995). Water speciation was not determined for most samples because spectra did not show measurable peaks at the 4,500 cm^-1 and 5,200 cm^-1 bands (Mcintosh et al., 2017). For the few samples with peaks detected at 1,630 cm^-1, spectra were analyzed using Spectragryph (v.1.2.16.1). Peak absorbance was determined on spectra corrected with adaptive baselines. Molecular water (H₂O_m) concentrations were calculated the Beer-Lambert law and the same parameters described above with a molar absorption coefficient of 25 ± 3 L/mol-cm (Dixon et al., 1995). Uncertainty was estimated by propagating errors through the Beer Lamber Law for sample thickness, density, absorption coefficient, and absorbance based on repeated analyses of the same site. Average precision (1-θ) for H₂O_t concentrations is 10%, which is consistent with previous studies of total water measurements made by FTIR (Dixon and Clague, 2001). Error for H₂O_m concentrations is higher because of additional uncertainty in absorbance intensity measured from adaptive baselines (McIntosh et al., 2022).

Most samples did not show a measurable CO₂ peak at ∼2,360 cm^-1, and the CO₂ peaks that were observed did not consistently appear in the spectra, even within the same chip. Therefore, CO₂ values are interpreted to be below the lower limit of quantification (20 ppm). The Supplementary Material contains the data for the few CO₂ peaks that were detected. The Beer-Lambert Law was used to calculate the CO₂ concentration using the same parameters described above and a molar absorption coefficient of 945 L/mol-cm for CO₂ (Fine and Stolper, 1985).

After FTIR analysis, 11 glass samples were carbon coated and analyzed for major elements by electron probe microanalysis (EPMA) at the University of Massachusetts Amherst. The Cameca SX 50 microprobe was operated under an acceleration voltage of 15 keV, a beam current of 20 nA, and a spot size of 30 µm. Full compositional data for the glass chips are provided in the (Supplementary Table SA1).

The alphaMELTS program (v. 1.9) was used to model crystallization and melting (Smith and Asimow, 2005). Using the MELTS thermodynamic model (Ghiorso and Sack, 1995), liquid lines of descent (LLD) were calculated for isobaric fractional crystallization at 1 kb and 1,200°C with 3°C steps. A primitive aphyric lava was used for the parent magma (VAT-SA-13-07, MgO 8.6 wt.%, La_N/Sm_N 1.44) with the addition of 0.5 wt.% H₂O. Initial Fe₂O₃ was calculated from FeO in alphaMELTS at the FMQ buffer. The same conditions were used to calculate the liquidus phase for two additional parent magma compositions (16MP02 and S-10-18 from Pollock et al., 2014). Using the pMELTS thermodynamic model (Ghiorso et al., 2002), mantle melts were generated through isentropic decompression melting starting at 4 GPa and 1,500°C with 0.01 GPa steps. Melting was continuous with 0.05% residual porosity. Two mantle source compositions were modeled: Depleted MORB mantle (Workman and Hart, 2005) and enriched mantle comprising 95% DMM and 5% pyroxenite from Koornneef et al. (2012). Trace element partition coefficients from McKenzie and O’Nions (1991), McKenzie and O’Nions (1995) remained constant during melting. Melts were aggregated using the 1D aggregation model and extracted at 2.17 GPa for both mantle sources.

VolatileCalc (v. 2.0) was used to calculate volatile saturation pressures (Newman and Lowenstern, 2002). Liquid temperatures were determined with alphaMELTS using glass or whole-rock compositions under the same conditions as the LLD models. Water concentrations were determined by FTIR. Because CO₂ solubility affects H₂O saturation pressures, pressures were calculated at 0 ppm and 15 ppm CO₂, representing complete and partial degassing. Full calculation data are provided in the (Supplementary Table SA8).

We have broken out several different lithofacies, including: 1) Pillow lava, 2) tuff, 3) lapilli tuff, 4) tuff-breccia, 5) dykes, 6) massive, columnar-jointed basaltic intrusions, 7) and diamict (Figures 2, 3). These lithofacies are essentially the same as those described in Pollock et al. (2014), and so are not described in detail here. The most common pillow-dominated units comprise stacked pillow lavas with very little intra-pillow material (Figure 4A). Tuff and lapilli tuff are limited to relatively thin interbeds between pillow units (Figure 4B), although they are more extensive locally on the eastern side of the ridge. Tuff-breccia is present in larger masses (Figures 3, 4C). Since the basic stratigraphy for Undirhliðar quarry was described by Pollock et al. (2014), here we focus on describing Vatnsskarð quarry and the ridge between the quarries.

Undirhliðar ridge is the northern extension of a much larger composite tindar ridge complex that extends for more than 20 km in total length (Figure 1). The northern half of the Undirhliðar segment is dominated by intact pillow lavas and pillow lava rubble (Figure 2C), which is sporadically directly overlain by a tan-brown, variably indurated diamicton interpreted to be of glacial origin. Approximately 1.5 km south of Undirhliðar quarry, the east side of the ridge abruptly shifts from pillow rubble to variably palagonitized lapilli tuff and tuff-breccia. Where they are in contact, the fragmental materials appear to directly overlie pillow lava units; however, the palagonitized tephra deposits are absent from either of the quarries. In several places small dykes (< 1 m thick) cut through the tephra-rich east side deposits and appear to be less common, although still present, in pillow units along the west-central part of the ridge (Figure 2C). Vatnsskarð quarry marks the southern end of the study area, where mining operations as of 2021 have bisected approximately half of the ridge width.

Vatnsskarð quarry, which is still active and expanding, is approximately 1 km long and up to 80 m from the quarry floor to the top of the ridge. Most of the Vatnsskarð quarry walls expose longitudinal sections of the ridge, but the northern end exposes a cross section that is perpendicular to the length of the ridge. We have identified 7 different pillow lava units based on stratigraphy and location, 4 different primary fragmental units (tuff, lapilli tuff, tuff-breccia), and overlying glaciofluvial deposits (tuff-breccia/diamict Figure 3). The north wall is dominated by pillow lavas, and because of their plunge orientations (see below), we have designated these pillows as a distinct unit (LpN; Figure 3).

The walls of Vatnsskarð quarry expose a continuous longitudinal section of the ridge, from the basal contact, through volcanic stratigraphy with multiple pillow and fragmental units, to capping sedimentary units (Figure 3). The basal contact is exposed near the center of the walls, where the lowest pillows (Lp1) appear in lenses that lie unconformably over sedimentary layers of yellow diamict containing cobble-sized clasts of vesicular basalt. The upper contact of the basal pillows lavas (Lp1) is marked by a thin (cm-scale) layer of vitric tuff and a sharp contact with overlying pillows (Lp2). Lp2 comprises the bulk of the central and southern quarry walls. Within the pillows are isolated lenses of lapilli tuff and vitric tuff-breccia that include glassy basaltic bombs. Above Lp2 is a dark black vitric tuff breccia (TB) that dips downward and thickens to the northeast. This fragmental unit consists of a vitric lapilli tuff (LT) with some highly vesicular glassy fragments that gradually coarsens to bomb-dominated, with glassy bombs that are mostly vesiculated throughout (LT-TB). The TB unit contains lobes of a third pillow unit (Lp3). The upper portion of the Lp3-TB complex is marked by a relatively flat-lying contact with a fourth pillow unit (Lp4) that hosts irregularly shaped intrusions, which are described in detail below. Capping the Lp4-intrusion complex is another pillow unit (Lp5). We lose stratigraphic control above this pillow unit and find one more isolated pillow exposure (Lp6) in a roadcut at the top of the mine. Laterally to the south, the volcanic stratigraphy is capped by a sequence of sedimentary units that lies unconformably over the exposures in the central and southern walls. Most of the sedimentary unit comprises a clast-rich sandy diamict that stands out in relief, containing ∼60% gravel-sized fragments and with weathered yellow to red appearance. Cobbles are rounded and striated. The matrix comprises glass and palagonitized sand-size grains. Within the sandy diamict is a 3 m-thick unit of gray muddy diamict with sparse interbedded sandy lenses.

Pillow units are distinguished based on their appearance and orientations. For example, Lp1 and Lp2 show a sharp contrast in appearance: Pillow lavas in Lp1 are aphyric, variably fractured, and weathered brown-yellow, whereas Lp2 pillows are darker, fresher-looking, olivine-bearing and have fresh glassy rinds with corrugated textures. Pillow orientations differ among the quarry walls (Figure 6). Lp2 pillows in the south wall plunge steeply to the southwest. Pillow units in the main quarry walls plunge to northwest. The north wall exposes a pillow unit (LpN) that plunges steeply to the south.

Irregular subhorizontal intrusions are present in all of the quarry walls (Figures 3, 5). They appear as laterally extensive massive columnar jointed basalts that are irregular in shape with complex jointing patterns. Many of the irregular intrusions show chilled margins and glassy contacts with the surrounding pillow lavas. The intrusions are holocrystalline with visible plagioclase, olivine, and clinopyroxene phenocrysts and crystal size increasing toward the interior. Some parts of the intrusions are slightly vesiculated (< 3%), although other locations along the margin have 10%–15% vesicularity, showing mm-scale vesicles, and sparse larger (4–5 mm) pipe vesicles. These irregular intrusions also contain gabbroic and troctolitic xenoliths. The xenoliths tend to appear at the base of the intrusions.

Ridge-parallel dykes cut through the pillow units on the southernmost and northernmost walls that expose cross-sections perpendicular to the ridge (Figure 3). The dykes are ∼1–1.5 m wide with chilled margins. They display well developed columnar joints and patterns in vesicularity (pipe vesicles perpendicular to margins and vesicle bands parallel to margins). The cores of some dykes are glassy, vesiculated, and fragmented. Ridge-perpendicular dykes are less abundant but also present.

In Undirhlíðar quarry, pillows in the central part of the quarry generally have southwest trends (236°–256°) with low plunges (Figure 6). These data are consistent with eruption from a vent trending perpendicular to the main ridge axis. However, pillows in the area to the south (pw07-pw10), have northwest trends (307°) with low plunges, suggesting an eruptive vent to the southeast. In Vatnsskarð quarry, a number of areas show pillows with plunge orientations that are also consistent with eruption from small fissures with a variety of orientations with respect to the main ridge axis (Figure 6). For example, pillows in the south wall (Lp2) show plunge directions opposite to pillows exposed in an erosional gully adjacent and south to the quarry.

Within the Undirhlíðar ridge suite, samples form distinct geochemical clusters defined by Rare Earth Element (REE) patterns (Figure 7). Based on relative light REE (LREE) enrichment, we divide the Undirhlíðar ridge samples into three compositional groups. Most of the suite comprises the “less-enriched” group with chondrite-normalized (McDonough and Sun, 1995) La_N/Sm_N less than 1.31. The “more-enriched” group overlaps the less-enriched group in REE abundance but has La_N/Sm_N ratios greater than 1.50. The “mixed” group has La_N/Sm_N ratios between 1.37 and 1.49 and shows the highest REE abundances in the suite. All of the Undirhlíðar ridge samples have smooth REE patterns with no or slightly positive Eu anomalies.

Undirhlíðar ridge REE data overlap with enriched lavas from the Reykjanes Peninsula but show a more restricted range in LREE enrichment (Figure 7). Reykjanes Peninsula lavas show La_N/Sm_N ranging from 1.20 to 1.67 (Kokfelt et al., 2006; Peate et al., 2009; Koornneef et al., 2012; Eason and Sinton, 2015; Halldórsson et al., 2016). Fagradalsfjall lavas show a wider range in La_N/Sm_N (1.24–2.74) and extend to lower REE abundances (Bindeman et al., 2022; Halldórsson et al., 2022). Using incompatible trace element ratios, Gee et al. (1998) divided Reykjanes Peninsula samples into “depleted” (Nb/Zr < 0.08) and “enriched” (Nb/Zr > 0.08) groups. Peate et al. (2009) further subdivided enriched historical Reykjanes Peninsula lavas into “less-enriched” (Nb/Zr 0.10–0.13, La_N/Sm_N 1.21–1.36) and “more-enriched” (Nb/Zr 0.13–0.14, La_N/Sm_N 1.38–1.48) groups based on incompatible trace element ratios and LREE enrichment. By these definitions, all of the Undirhlíðar ridge samples are enriched. Like Peate et al. (2009), we observe more-enriched and less-enriched subdivisions within the Undirhlíðar ridge dataset. Our more-enriched group shows higher La_N/Sm_N values than the more-enriched group of Peate et al. (2009). Our mixed group would have been classified by Peate et al. (2009) as “more-enriched,” but we choose to separate the mixed samples because of compositional differences.

The three compositional groups show variations that are distinguishable in major element space (Figure 8). In general, with decreasing MgO, the Undirhlíðar ridge suite shows decreasing Al₂O₃ and CaO, increasing FeO^T, TiO₂, and Na₂O, and relatively flat SiO₂ values. The less-enriched group encompasses the entire range of MgO found in the dataset, extending to the highest MgO values (MgO >9.0 wt.%). The high-MgO samples are dominated by olivine-phyric intrusions and pillow lavas. At a given value of MgO, some less-enriched samples show elevated Al₂O₃ and CaO and lower FeO^T and K₂O. These samples are plagioclase-phyric pillow lavas. The mixed and more-enriched groups are distinguished by where they overlap with the less-enriched group. Mixed group samples dominate the low-MgO range of the Undirhlíðar ridge dataset. More-enriched samples fall toward the lower edges of TiO₂, FeO^T, and Al₂O₃ fields and the higher edges of CaO field defined by the less-enriched samples. The most notable distinction among the three compositional groups is in K₂O. For a given value of MgO, the more-enriched group shows the greatest variability in K₂O and extends to higher values. This distinction is clearly observed in the ratio of K₂O/TiO₂, where the more-enriched group shows the highest values (avg. 0.18 ± 0.04, n = 25), the less-enriched group shows the lowest values (avg. 0.10 ± 0.03, n = 107), and the mixed group spans the range of the suite.

Overall, the Undirhlíðar ridge samples are tholeiitic basalts similar in major element composition to other lavas from the Reykjanes Peninsula (Jakobsson et al., 1978; Condomines et al., 1983; Hemond et al., 1988; Hemond et al., 1993; Gee et al., 1998; Kempton et al., 2000; Skovgaard et al., 2001; Fitton et al., 2003; Momme et al., 2003; Kokfelt et al., 2006; Maclennan, 2008; Peate et al., 2009; Jakobsson and Johnson, 2012; Koornneef et al., 2012; Eason and Sinton, 2015; Halldórsson et al., 2016). Reykjanes Peninsula samples span a slightly wider range in MgO compared to Undirhlíðar ridge (Figure 8). Like the Undirhlíðar compositional groups, the less- and more-enriched compositional groups of Peate et al. (2009) are distinct in major elements. Namely, the less-enriched group shows lower MgO, K₂O, and TiO₂ and higher SiO₂ and Fe₂O₃ than the more-enriched group (Peate et al., 2009). Although we observe that our less-enriched samples are lower in K₂O than our more-enriched samples, the other patterns identified by Peate et al. (2009) do not apply to the Undirhlíðar ridge data. Our less-enriched samples are higher in TiO₂ and lower in SiO₂ compared to our more-enriched samples (Figure 8). Our compositional groups span most of the range of MgO values (Figure 9A) and show no correlation with FeO^T (Figure 9B).

The Undirhlíðar ridge dataset shows positive correlations between LREE and incompatible trace element enrichment (Figure 9). The more-enriched samples have higher incompatible trace element ratios (Zr/Y 3.6-4.0) compared to the less-enriched group (Zr/Y 3.1-3.6). The mixed samples have incompatible trace element ratios that fall between the more- and less-enriched groups. Undirhlíðar ridge samples overlap with enriched samples from the Reykjanes Peninsula, which encompass greater ranges in incompatible trace element ratios (Wood et al., 1979; Chauvel and Hémond, 2000; Peate et al., 2009; Koornneef et al., 2012; Eason and Sinton, 2015; Halldórsson et al., 2016).

The three compositional groups are correlated with spatial location along the ridge. Almost all of the more-enriched samples are found in the basal stratigraphic units at lower elevations in Undirhlíðar quarry. Mixed samples are the least abundant in the suite and most are located along the ridge between the quarries. The less-enriched group is the most abundant in the suite, found in the dykes and upper units in Undirhlíðar quarry, along the ridge, and heavily concentrated in Vatnsskarð quarry. The single sample from the basal, weathered unit in Vatnsskarð quarry is compositionally distinct from the rest of the suite with a much higher Nb/Zr ratio (Figure 9).

Within the quarries, we observe patterns in trace element compositions related to lithostratigraphic units. Almost all of the Vatnsskarð quarry extrusive samples belong to the less-enriched group; the exceptions are two mixed-group samples (a bomb from a tuff breccia unit and a single pillow lava). Within the less-enriched extrusive units, we observe a shift in trace element ratios that correlates with a stratigraphic break between exposures from north to south. Pillow lavas in the north wall show identically low values of La_N/Sm_N (1.20). Pillow lavas in the other Vatnsskarð quarry exposures show a range of La_N/Sm_N values that encompasses most of the range of the less-enriched suite (1.21–1.27). The transition between north wall and the rest of the Vatnsskarð quarry occurs over a distance of tens of meters. In general, Vatnsskarð quarry intrusions show similar REE patterns and abundances to the pillows into which they intrude. However, in Undirhlíðar quarry, less-enriched dykes intrude through more-enriched pillow lavas in the lower stratigraphic units.

Undirhlíðar ridge radiogenic isotope compositions (Sr-Nd-Pb) encompass a narrow range that overlaps with isotopically enriched lavas from the Reykjanes Peninsula (Table 2; Figure 10; Schilling, 1973; Sun and Jahn, 1975; Condomines et al., 1983; Hemond et al., 1993; Gee et al., 1998; Kempton et al., 2000; Fitton et al., 2003; Thirlwall et al., 2004; Kokfelt et al., 2006; Peate et al., 2009). Within dataset limits, Undirhlíðar ridge is consistent with several isotopic relationships observed in other lavas from the Reykjanes Peninsula. First, radiogenic isotopes show positive correlations with trace element ratios (Peate et al., 2009). Although six of the seven Undirhlíðar ridge samples are from the less-enriched compositional group, the single more-enriched sample shows greater ²⁰⁶Pb/²⁰⁴Pb (Figure 10). Second, in their suite of historical Reykjanes Peninsula lavas, Peate et al. (2009) observed that their less- and more-enriched compositional groups were nearly identical in radiogenic Nd and Sr compositions and showed linear correlations in Pb-Pb isotope space. With the exception of a pillow lava from the upper units at Undirhlíðar quarry (S-10-23), the Undirhlíðar ridge samples also overlap in ¹⁴³Nd/¹⁴⁴Nd and ⁸⁷Sr/⁸⁶Sr compositions and show linear Pb-Pb isotope patterns (Figure 10). Third, Peate et al. (2009) observed that the Reykjanes Peninsula data plot below the Northern Hemisphere Reference Line (NHRL) for ²⁰⁷Pb/²⁰⁴Pb (negative ∆ ²⁰⁷Pb) and above the NHRL for ²⁰⁸Pb/²⁰⁴Pb (positive ∆ ²⁰⁸Pb). All of the Undirhlíðar ridge samples show negative ∆ ²⁰⁷Pb values, forming a linear trend that extends toward more positive values. The Undirhlíðar ridge samples also show ∆ ²⁰⁸Pb values that are positive or near zero.

On Pb-Pb isotope plots, the less-enriched Undirhlíðar ridge samples create a linear array (Figure 10). The ends of the linear array are bracketed by samples from Vatnsskarð quarry, with the least isotopically enriched sample from the southern end and the most isotopically enriched sample from <1 km away in the northern end. Samples from the upper stratigraphic units of Undirhlíðar quarry fall between the Vatnsskarð quarry samples. The single sample from the more-enriched group represents the lower stratigraphic units in Undirhlíðar quarry. Although this sample clusters with the less-enriched samples on a plot of ¹⁴³Nd/¹⁴⁴Nd vs. ⁸⁷Sr/⁸⁶Sr, it falls below the linear trend defined by the Vatnsskarð endmembers Pb-Pb isotope plots. The more-enriched sample also has the most negative ∆ ²⁰⁷Pb and lowest ∆ ²⁰⁸Pb values in the sample suite.

Water concentrations for Undirhlíðar ridge were analyzed from fresh glass chips that showed vitreous surface textures, sparse plagioclase microlites, and vesicularity <20% (Table 3; Figure 11). Water speciation was not determined for most samples, so measurements represent total water (H₂O_t) concentration. FTIR mapping reveals homogeneous water concentrations within the glass. Highest water concentrations are observed around fractures and vesicles, which were avoided during data acquisition (Supplementary Figure SA1). Only five of the 22 samples produced a detectable peak CO₂ peak at the 2,360 cm^-1 position, indicating that measured CO₂ values are at or below detection limits (< 20 ppm).

To check if water concentrations represent magmatic conditions, we measured water speciation when possible. Only five samples produced measurable H₂O_m peaks at the 1,630 cm^-1 band (Table 3). Secondary hydration enriches volcanic glasses in H₂O_m (e.g., Mcintosh et al., 2017). Most samples did not show measurable H₂O_m. For the few samples that showed measurable peaks, H₂O_m/H₂O_t ratios are less than the values found in experiments of basaltic glasses quenched at high temperatures (Dixon et al., 1995), suggesting that the analzyed glasses in this study did not experience secondary hydration (e.g., Sano and Yamashita, 2019). To determine if water concentrations from a single pillow represent the conditions for surrounding lavas, we conducted detailed sampling of adjanced pillow lavas and assessed small-scale (< 1 m) spatial variations in H₂O_t concentrations (Figure 11). The four samples taken from the same pillow in Undirhlíðar quarry have measured H₂O_t concentrations that are similar within analytical error (Table 3). Likewise, the samples from the cluster of adjacent pillows are within analytical error of one another. Therefore, we find that the H₂O_t data measured by FTIR on individual pillow lavas are reproducible and representative of the unit in which the pillow lava was erupted.

Water concentrations for Undirhlíðar ridge span a wide range (0.16–0.40 wt.%) and generally decrease with increasing elevation (Figure 11). We observe the greatest range of water contents (0.19–0.36 wt.%) at ∼145 m elevation. Water concentrations are most variable over the smallest spatial scales in Undirhlíðar quarry, where contents change from 0.23–0.40 wt.% H₂O over walls that are ∼50 m high and ∼150 m long. Conversely, Vatnsskarð quarry is dominated by less-enriched samples and shows a narrower range of H₂O concentrations (0.24–0.31 wt.%), despite exposing walls that are taller (∼80 m) and longer (∼750 m).

Calculated water saturation pressures mimic the pattern of water concentrations (Figure 11). Assuming complete CO₂ degassing, saturation pressures range from 0.3 MPa to 1.6 MPa. Using densities of 0.917 g/cm³ for ice and 1.000 g/cm³ for water, saturation pressures correspond to ice thicknesses up to 178 ± 33 m and water depths up to 163 ± 31 m. The decrease in saturation pressure with elevation generally follows a linear trend predicted by glaciostatic conditions under 200 m-thick ice. However, most less-enriched samples between ∼120 m and ∼180 m in elevation fall below the glaciostatic curve.

The significant decrease in water contents starting at ∼120 m in elevation is correlated with a shift in trace element ratios (Figure 11). More-enriched samples show greater H₂O concentrations (average 0.37 ± 0.03 wt.%, n = 12) and less-enriched samples show lower H₂O concentrations (average 0.25 ± 0.04 wt.%, n = 25). To examine the influence of degassing and magma differentiation on water contents, we compared H₂O to Ce, a trace element that behaves similarly during magmatic processes (e.g., Sano and Yamashita, 2019). Water contents show a positive linear correlation with Ce. Less-enriched samples show a wide range in H₂O/Ce ratios (average 153 ± 24, n = 20). Samples from the mixed and more-enriched groups fall along a line with a slope that matches the H₂O/Ce ratio of the less-enriched group.

Compositional data indicate that mantle source and crustal processes both play essential roles in the formation and evolution of magma at Undirhlíðar ridge. Some variability in major element and REE patterns is consistent with the effects of crystallization and crystal accumulation (Figures 7, 8). This is demonstrated in the major element trends of increasing FeO^T, TiO₂, and Na₂O and decreasing Al₂O₃ and CaO with decreasing MgO. The most evolved samples in the suite show the greatest REE abundances. The effects of crystal accumulation are apparent in olivine-phyric lavas that show elevated MgO and plagioclase-phyric lavas that show elevated Al₂O₃ and positive Eu anomalies.

The observed compositional variations are consistent with thermodynamic models of fractional crystallization (Figures 7, 8). Isobaric shallow fractional crystallization of a primitive parent magma from the mixed group shows a typical basaltic crystallization sequence of ol, ol + pl, and ol + pl + cpx. The resulting LLD forms downward curving paths in Al₂O₃ and CaO and linear upward paths in FeO^T, TiO₂, and Na₂O that follow major element patterns. REE abundances can also be explained by varying degrees of crystallization, which do not affect the slope of REE patterns but cause relative REE abundances to increase in more evolved lavas. The higher REE abundances of the mixed samples can be generated by up to 30% crystallization. Much of the scatter in major element and REE patterns can be explained by variable degrees of crustal-level crystallization.

While all of the Undirhlíðar ridge magmas evolved in the crust, the samples cannot be related to each other by cooling of a single parent magma. This is demonstrated by the scatter in major and trace elements, particularly in SiO₂, K₂O, K₂O/TiO₂, and La_N/Sm_N at a given value of MgO (Figures 8, 9). More-enriched samples follow major element trends that parallel the modeled LLD at lower values of TiO₂, FeO^T, and Al₂O₃ and higher values of CaO, suggesting a different parent magma composition. Separate parent magmas are also indicated by modeled liquidus phases. For parent magmas from the from the mixed group (VAT-SA-13-07) and the less-enriched group (16MP02), the modeled liquidus phase is olivine; for a parent magma from the more-enriched group (S-10-18), the liquidus phase is clinopyroxene. In Pollock et al. (2014), we argued that the less-enriched and more-enriched groups follow separate LLD and proposed a model for crystallization in separate crustal reservoirs. At that time, we had not identified the mixed samples from the ridge. Our expanded dataset confirms that the Undirhlíðar ridge magmas cannot be derived from crystallization of a single parent magma in the same melt reservoir. The major and trace element variability are consistent with variations in mantle melting or source composition underlying Undirhlíðar ridge.

In Pollock et al. (2014), we argued that the compositional variations in Undirhlíðar quarry could be explained by mixing of mantle melts extracted from over a range of depths, but our expanded study shows that the compositional groups are likely related to mantle heterogeneity. In our expanded dataset, we observe no correlation between La_N/Sm_N and FeO^T (Figure 9), a major element indicator of degree and pressure of melting. Undirhlíðar ridge samples also have smooth REE patterns with no difference in degree of HREE fractionation between the compositional groups (Figure 7), suggesting a relatively constant degree of melting from shallow depths. Instead of variations in melting of a homogeneous mantle source, the variability in Pb isotopes in our expanded dataset demonstrate that the source mantle cannot be a single homogeneous composition.

Mantle source heterogeneity must influence the compositional variability in the Undirhlíðar ridge magmas. Variable enrichment in incompatible elements and radiogenic isotopes in Iceland have been attributed to aggregation of melts from heterogeneous mantle that are extracted over a range of depths (Hanan and Schilling, 1997; Chauvel and Hémond, 2000; Hanan et al., 2000; Kempton et al., 2000; Stracke et al., 2003; Thirlwall et al., 2004; Thirlwall et al., 2006; Kokfelt et al., 2006; Peate et al., 2009; Koornneef et al., 2012). On the Reykjanes Peninsula, linear isotopic trends and correlations between isotopes and trace element indicators of enrichment have been interpreted as near-binary mixing between mantle sources (Thirlwall et al., 2004; Kokfelt et al., 2006; Peate et al., 2009). The presence of up to six mantle endmembers has been suggested by previous workers (Murton et al., 2002; Thirlwall et al., 2004; Kokfelt et al., 2006; Peate et al., 2009). The nature and origin of the mantle heterogeneity is discussed by numerous workers, but many posit that there are enriched components related to the plume and the alkalic source and depleted components related to the ambient mantle (Kempton et al., 2000; Murton et al., 2002; Thirlwall et al., 2004; Kokfelt et al., 2006). Here, we use simple binary mixing equations (Langmuir et al., 1978) to calculate mixing curves among four endmembers: two enriched mantle compositions are defined by the enriched plume (represented by Eldgja (E) and alkalic Snaefellsnes (S) lavas) and two depleted mantle sources that are similarly depleted in trace elements but show different isotopic compositions (Murton et al., 2002; Thirlwall et al., 2004; Kokfelt et al., 2006).

The Undirhlíðar Pb-Pb isotope data create a linear array that we interpret as mixing between two mantle source compositions. The mixing trends are best seen on the ∆²⁰⁷Pb and ²⁰⁷Pb/²⁰⁴Pb plots, where the mixing lines between the Eldgjá and depleted endmembers are most distinct (Figure 10). The Undirhlíðar data form a binary mixing line between two mantle compositions that are intermediate between the endmembers. The less-enriched samples trend toward one endmember that is a mix of Eldgjá and D2. The more-enriched sample trends toward the second endmember that is a mix between Eldgjá and D1. Because the Snæfellsnes endmember is itself intermediate between Eldgjá and D1, it is difficult to determine the role of the Snæfellsnes source using the isotope data. The location of Snæfellsnes on a mixing line between Eldgja and D1 suggests that the alkalic source may make a bigger contribution to the more-enriched samples. This is consistent with observations on plots of trace element ratios, where binary mixing creates hyperbolas whose curvatures are determined by a ratio of the endmember denominators (Figure 9). On plots of La_N/Sm_N versus Zr/Y and Nb/Zr versus Zr/Y, all of the Undirhlíðar ridge data fall within a multi-component mixing array defined by the Eldgjá, Snæfellsnes, and depleted mantle components. The more-enriched samples fall toward an enriched endmember that is intermediate between Snæfellsnes and the depleted endmembers. The less-enriched samples fall toward an endmember that is intermediate between the Eldgjá and depleted endmembers.

To test whether a heterogeneous mantle source can produce the range of La_N/Sm_N values that we observe in the Undirhlíðar ridge data, we modeled polybaric continuous melting for two mantle sources under the same conditions using AlphaMelts. One mantle source is the depleted mantle (DMM) from Workman and Hart (2005). The other mantle source is DMM that has been enriched in pyroxenite (Koornneef et al., 2012). Melts from the two mantle sources reproduce REE patterns observed at Undirhlíðar ridge (Figure 7). The depleted mantle melt overlaps with REE for the less-enriched group. The melt from the DMM enriched with pyroxenite overlaps with REE for the more-enriched group. This suggests that the difference in La_N/Sm_N ratio can be generated by different mantle source compositions that melt under similar conditions. To generate the trace element trends with comparatively constant degrees of melting, the more-enriched samples require a higher amount of the enriched mantle component, which we also observe in our isotopic and trace element ratio data.

Our understanding of the nature of the magma plumbing system can be informed by the relationship between crystallization and mixing of heterogeneous mantle melts. Because the curvature of a mixing hyperbola in plots of incompatible trace element ratios depends on the denominators of the endmembers, mixing should result in a linear array on a plot of 1/Y versus Zr/Y (Langmuir et al., 1978). Undirhlíðar ridge data fall off a linear array as a result of variable degrees of crystallization, with the most evolved lavas extending to the lowest values of 1/Y (Figure 9D). Mixing must have occurred prior to crystallization. This is consistent with major elements trends, where the compositional groups must have had parent magma compositions that differed in CaO, SiO₂, and K₂O (Figure 8). The magma plumbing system preserves mantle source signatures on small spatial scales. Within the area exposed by Undirhlíðar quarry, we observe more-enriched lavas intruded by less-enriched magmas. Vatnsskarð quarry is dominated by the less-enriched group but shows geographic shifts in LREE enrichment within the northernmost exposures. The mixed group is the most evolved, suggesting that it was cooled to greater degrees. Because this compositional variability is preserved, even at the local scale, there must be no large-scale efficient mixing processes to homogenize the magma. We propose that the magmatic plumbing system consisted of separately evolving crustal melt bodies and that original model from Pollock et al. (2014) extends to the entire ridge.

Paleo-ice conditions for Undirhlíðar ridge are constrained by the measurements of water in quenched glassy pillow rims. Glass textures and variations in volatile content show evidence of volatile saturation and degassing. The glasses show abundant vesicles, suggesting degassing of a volatile saturated magma (Tuffen et al., 2010). Because CO₂ degasses more readily than H₂O, and measured CO₂ concentrations are at or below the detection limits, CO₂ was essentially entirely degassed when the glasses were quenched (Dixon and Stolper, 1995). Although it is possible that vesicles represent predominately CO₂ bubbles that formed before H₂O degassing, samples with low H₂O/Ce ratios indicate that H₂O degassing has occurred in the Undirhlíðar suite. Post-emplacement hydration has not affected H₂O contents presented in this study. Although higher H₂O concentrations were observed in the fractures, we avoided fractures while measuring. The lack of measurable H₂O_m peaks and low H₂O_m/H₂O_t ratios suggest that molecular water was not enriched by secondary hydration. Thus, we infer that the Undirhlíðar ridge magmas degassed prior to quenching and that H₂O concentrations are indicative of pressures during emplacement.

Calculated saturation pressures suggest that Undirhlíðar ridge formed within ice at least 200 m thick. The range of water contents and emplacement pressures at Undirhlíðar ridge is similar to those observed in other subglacial edifices on the Reykjanes Peninsula (Nichols et al., 2002; Schopka et al., 2006). At Helgafell, a Pleistocene-age hyaloclastite ridge ∼1 km east of this study, ice thickness was estimated to be ∼500 m at the time of eruption, although volatile contents indicated lower emplacement pressures caused by meltwater drainage and ice subsidence (Schopka et al., 2006). Estimates of ice thickness on the Reykjanes Peninsula during the last glacial maximum range from 250 m to 500 m (Einarsson et al., 1988; Licciardi et al., 2007; Le Breton et al., 2010; Patton et al., 2017).

A major change in water contents at Undirhlíðar ridge correlates with a shift in the magmatic system. The more-enriched lavas show higher H₂O contents than the less-enriched lavas, which is likely due to differences in magma composition. The geochemical groups have similar H₂O/Ce ratios, indicating that the mixed and more-enriched samples have not experienced more degassing than the less-enriched samples. The positive linear correlation between H₂O and Ce suggests that water is behaving as an incompatible element. We interpret the shift from wetter, more-enriched lavas to less-wet, less-enriched lavas as a result of a shift in melts from a more enriched mantle to a more depleted mantle.

However, within the less-enriched group, lavas show variable extents of degassing. Less-enriched lavas with lower H₂O/Ce ratios have undergone more degassing than those with higher values. Many of the less-enriched samples show saturation pressures lower than expected for glaciostatic conditions. These less-enriched lavas show wide variations in water contents, saturation pressures, and H₂O/Ce ratios over short distances (∼100 s of m) at mid-elevations along the ridge. For this group of less-enriched lavas, hydrologic conditions were dynamic during emplacement.

Ice conditions varied during construction of Undirhlíðar ridge. Saturation pressures suggest that Undirhlíðar ridge erupted under thin ice, similar to conditions at Grímsvötn and Eyjafjallajökull (Magnússon et al., 2012). The initial summit eruption in the 2010 Eyjafjallajökull event occurred under ∼200 m thick ice, leading to high subglacial water pressures associated with localized glacier uplift and accumulation of meltwater in an ice cauldron (Magnússon et al., 2012). Accumulated water was released in supraglacial flooding that lowered water levels and reduced emplacement pressures (Magnússon et al., 2012). Within days, flank eruptions extending ∼1 km from the summit experienced different hydrologic conditions. Flank eruptions occurred on steeper slopes under thinner (50–100 m thick) ice, resulting in rapid drainage of meltwater through high volume, short duration flood events (Magnússon et al., 2012) that created localized water-drained areas with low emplacement pressures (Woodcock et al., 2016). The dynamic variability in hydrologic conditions at Eyjafjallajökull over km-long spatial scales and days-long temporal scales is consistent with the variable extents of degassing observed in the less-enriched lavas that comprise the bulk of the ridge at Undirhlíðar. Saturation pressures return to values consistent with glaciostatic conditions in the upper elevations of Undirhlíðar ridge, suggesting that the upper portions of the edifice were emplaced beneath ice or in a stable englacial lake. The presence of ice at the upper reaches of the ridge is also illustrated by the diamict that drapes over Vatnsskarð quarry, which is consistent with a recovery or return of ice after eruptions ceased.

Our detailed study of the compositions and lithostratigraphic relationships allows us to propose several revisions to the existing models for the construction of glaciovolcanic fissure-fed eruptions. We observe a full vertical section of Undirhlíðar ridge in Vatnsskarð quarry. The basal contact of the ridge lies uncomformably over older palagonitized tuff-breccia, pillow lavas and local glaciofluvial deposits. The sandy and muddy diamict units draping over the central and southern walls of the quarry, in addition to the remnant till deposits scattered along the length of the ridge top, suggest that the pillow ridge was covered by a glacier after the eruption. We infer that the ∼3 km length of the ridge was emplaced in an ice-confined environment through a series of fissure eruptions.

Eruptions were fed by multiple vents (Figure 12). Plunges reveal that many of the pillows were erupted from vents that parallel the strike of the ridge, but exposures in quarry walls also show eruptive vents and pillow emplacement that were ridge-perpendicular (Figure 6). An example of this is the north wall of the Vatnsskarð quarry, in which the plunge directions in the north wall pillows suggest that this is an isolated “nose” of pillows that erupted off the main ridge axis. The north wall pillow lavas are also compositionally distinct from the other eruptive units in Vatnsskarð quarry, suggesting that the north wall pillows form their own distinct pillow mound within the broader ridge structure.

Within the growing edifice, magma was transported in a complex intrusive system (Figure 12). Some dykes are ridge-parallel and cut through pillows that belong to a different compositional group, suggesting that dykes played an important role in transporting magma along-axis. Irregular intrusions are exposed in both Undirhlíðar ridge and in Vatnsskarð quarry. Some have open tube structures and others show evidence of collapsed tube structures, such as shelves and lava drips that are typical of lava tubes in subaerial and glaciovolcanic systems (Hungerford et al., 2014). The irregular and massive intrusions frequently are the same composition as the lavas into which they intrude. We interpret these to be part of the shallow plumbing system of the growing pillow edifice, which were important for distributing magma locally.

Emplacement conditions and the magma source changed as the edifice grew. Eruptions forming the lowermost units were fed by more-enriched mantle melts emplaced into a ∼200 m thick ice sheet under glaciostatic conditions. Eruptions forming the bulk of the ridge were fed by less-enriched mantle melts. These less-enriched lavas degassed to variable extents under dynamically shifting hydrologic conditions along the length of the ridge. Less-enriched melts continued to feed eruptions forming the uppermost units, where emplacement conditions were glaciostatic.

We originally proposed a sequence of events for the construction of the volcanic succession exposed at Undirhlíðar quarry that included multiple eruptive and intrusive phases (Pollock et al., 2014). This study expands on previous work by adding detailed lithostratigraphic mapping of Vatnskarð quarry, additional major and trace element data, and new volatile and isotope analyses. Using the field relationships and geochemical findings from this study, we extend the model to the formation of Undirhlíðar ridge that is summarized as follows (Figure 13):

1. The entire ridge was emplaced upon a glaciated surface of pre-existing glaciovolcanic deposits, presumably from an early glaciation. Limited exposures show palagonitized tuff-breccia unconformably overlain by discontinuous gravels.

By sampling and mapping Undirhlíðar ridge at a high-resolution, we are able to test general models for the construction of tindar ridges. Our study confirms some aspects of the theoretical models, namely, that 1) pillow-dominated tindar ridges are built through a complex sequence of eruptive phases from multiple eruptive vents that show changing eruptive styles (effusive vs. explosive) and 2) hydrologic conditions are dynamic on small spatial scales. Our study also adds new insights into the enigmatic aspects of the theoretical models, namely, that shallow-level intrusions are important to distributing lava within the growing pillow edifice.

The 2021–22 eruptions at Fagradalsfjall, which is located on the volcanic system adjacent to the western side of Krýsuvík, allows us to use direct observations of a subaerial fissure eruption to surmise details that cannot be observed in subglacial environments. At Undirhlíðar ridge, pillow orientations and compositions provide evidence for multiple eruptive vents, but it is not possible to know the number or spacing of active vents. Variations in stratigraphic packages are consistent with numerous eruptive pulses, but it is difficult to determine the duration of the Undirhlíðar ridge eruption. Volcanic activity at Fagradalsfjall lasted for ∼6 months, followed by a ∼2-week eruption nearly a year later (Pedersen et al., 2022). At least five eruptive vents opened along a ∼2 km long fissure segment (Bindeman et al., 2022; Pedersen et al., 2022). Volcanic activity pulsated and eruption style shifted between effusive lava extrusion and more explosive fire fountaining (Bindeman et al., 2022; Halldórsson et al., 2022). The resulting lava field covers an area of ∼5 km² with a DRE volume of ∼0.1 km³ (Bindeman et al., 2022) and an average estimated thickness of 30 m (Pedersen et al., 2022) Like Fagradalsfjall, Undirhlíðar ridge was built by a moderately-sized eruption that occurred along a fissure segment on the order of 3–4 km long, and has an area of about 4.3 km². Pillow-dominated tindars like Undirhlíðar ridge are interpreted to be the result of short-duration, small-volume monogenetic events (Jakobsson and Johnson, 2012). Such events have been observed in modern glaciovolcanic eruptions at Eyjafjallajökull (2010) and Gjalp (1996) (Thordarson and Larsen, 2007; Gudmundsson et al., 2012). Despite the difference in eruptive environments, the spatial and temporal scales of the Fagradalsfjall eruption may be similar to the tindar-building fissure eruption that constructed Undirhlíðar ridge.

Direct geophysical and petrological observations at Fagradalsfjall yield insights into the processes that initiated the Undirhlíðar ridge eruption. At Undirhlíðar ridge, lavas with different mantle source signatures were erupted sequentially from separate crustal melt reservoirs, suggesting that the main ridge-building event was triggered by injection of magma into the crustal plumbing system. At Fagradalsfjall, the eruption was fed from a lower crustal magma reservoir at near-Moho (∼15–20 km) depths, supplied with chemically variable melts from a heterogeneous mantle (Bindeman et al., 2022; Halldórsson et al., 2022). Erupted lava compositions at Fagradalsfjall progressively transitioned to more enriched mantle melts (Bindeman et al., 2022; Halldórsson et al., 2022). The addition of enriched melts to a deep crustal magma reservoir may have caused a mixing event that initiated magma ascent and eruption (Halldórsson et al., 2022). In the months leading up to the Fagradalsfjall eruption, seismic swarms and surface inflation were attributed to subsurface magma migration (Cubuk-Sabuncu et al., 2021; Geirsson et al., 2021; Sigmundsson et al., 2022). At least a year prior to the geophysical signals of volcano-tectonic unrest, the deep magma chamber experienced a disequilibrium event (Kahl et al., 2022). Diffusion modeling of olivine and plagioclase crystals suggests that the onset of disequilibrium in the deep magma chamber was related to magma injection and mush disaggregation (Kahl et al., 2022). At both Fagradalsfjall and Undirhlíðar ridge, the supply of heterogeneous mantle melts to the deep parts of the magmatic system played a critical role in initiating eruptions (e.g., Kahl et al., 2022).

The relative locations of the Krýsuvík andFagradalsfjall volcanic systems allows us to comment on spatial variations in mantle composition under the Reykjanes Peninsula. Bindeman et al. (2022) identified at least three different mantle components in the Fagradalsfjall lavas and proposed a lateral gradient in degree of mantle enrichment, in the context of the “plume sheath” suggested by previous researchers (Fitton et al., 1997; Kempton et al., 2000; Murton et al., 2002). The laterally variable plume sheath model predicts that Krýsuvík should erupt lavas more enriched in incompatible trace elements and radiogenic isotopes (Fitton et al., 1997; Kempton et al., 2000; Murton et al., 2002; Bindeman et al., 2022). We find no evidence for a systematic change in mantle composition between Fagradalsfjall and Undirhlíðar ridge. Undirhlíðar ridge has more radiogenic ²⁰⁶Pb/²⁰⁴Pb and ²⁰⁸Pb/²⁰⁴Pb than Fagradalsfjall, but Sr-Nd isotopes do not show the same enrichment. Fagradalsfjall incompatible trace element ratios overlap with and extend beyond the Undirhlíðar ridge data. The Undirhlíðar ridge and Fagradalsfjall eruptions capture magmatic conditions for moments in time, reflecting complex interactions among the scale of mantle source heterogeneity, the region of melt generation, and the mechanism of melt extraction (e.g., Peate et al., 2009). A more appropriate evaluation of the lateral plume sheath model should examine the full range of trace element and isotope compositions erupted at each of the volcanic systems on the Reykjanes Peninsula over the longest available time frames (e.g., Gee et al., 1998; Peate et al., 2009).