Evidence for Cyclical Fractional Crystallization, Recharge, and Assimilation in Basalts of the Kimama Drill Core, Central Snake River Plain, Idaho: 5.5-Million-Years of Petrogenesis in a Mid-crustal Sill Complex

Basalts erupted in the Snake River Plain of central Idaho and sampled in the Kimama drill core link eruptive processes to the construction of mafic intrusions over 5.5 Ma. Cyclic variations in basalt composition reveal temporal chemical heterogeneity related to fractional crystallization and the assimilation of previously-intruded mafic sills. A range of compositional types are identified within 1,912 m of continuous drill core: Snake River olivine tholeiite (SROT), low K SROT, high Fe-Ti, and evolved and high K-Fe lavas similar to those erupted at Craters of the Moon National Monument. Detailed lithologic and geophysical logs document 432 flow units comprising 183 distinct lava flows and 78 flow groups. Each lava flow represents a single eruptive episode, while flow groups document chemically and temporally related flows that formed over extended periods of time. Temporal chemical variation demonstrates the importance of source heterogeneity and magma processing in basalt petrogenesis. Low-K SROT and high Fe-Ti basalts are genetically related to SROT as, respectively, hydrothermally-altered and fractionated daughters. Cyclic variations in the chemical composition of Kimama flow groups are apparent as 21 upward fractionation cycles, six recharge cycles, eight recharge-fractionation cycles, and five fractionation-recharge cycles. We propose that most Kimama basalt flows represent typical fractionation and recharge patterns, consistent with the repeated influx of primitive SROT parental magmas and extensive fractional crystallization coupled with varying degrees of assimilation of gabbroic to ferrodioritic sills at shallow to intermediate depths over short durations. Trace element models show that parental SROT basalts were generated by 5–10% partial melting of enriched mantle at shallow depths above the garnet-spinel lherzolite transition. The distinctive evolved and high K-Fe lavas are rare. Found at four depths, 319, 1045, 1,078, and 1,189 m, evolved and high K-Fe flows are compositionally unrelated to SROT magmas and represent highly fractionated basalt, probably accompanied by crustal assimilation. These evolved lavas may be sourced from the Craters of the Moon/Great Rift system to the northeast. The Kimama drill core is the longest record of geochemical variation in the central Snake River Plain and reinforces the concept of magma processing in a layered complex.

Introduction

The relationship between volcanic rocks erupted on Earth's surface and their putative plutonic roots is a long-standing geologic problem (e.g., Bachmann et al., 2007; Annen et al., 2015; Cashman et al., 2017). The petrologic and chemical evolution of volcanic provinces and the formation of continental crustal plutonic complexes are typically studied in isolation from one another, yet each of these topics has implications for the other related to magmatic flux, intrusion geometries, fractionation mechanisms, and the effects of partial melting and assimilation (Annen et al., 2015). Previous efforts to understand linkages between pluton construction and eruptive processes have focused largely on silicic systems: the assembly of granitic batholiths and rhyolite ignimbrite eruptions (e.g., Lipman, 1984; Metcalf, 2004; Annen et al., 2006). Although large mafic layered intrusions have been studied extensively (e.g., Irvine, 1970) and the effect of basalt intrusions on crustal heat flux has been modeled (Annen and Sparks, 2002), there are few studies that infer mafic plutonic evolution from basalt compositions in long-lived mafic volcanic provinces (e.g., Shervais et al., 2006). In this paper we use the petrologic and geochemical evolution of basalt recovered in drill core to infer crustal magmatic processes over 5.5 Ma of mafic volcanism in continental crust.

The Snake River Plain (SRP) of central Idaho is a manifestation of Yellowstone-Snake River Plain (YSRP) hotspot volcanism and contains intriguing evidence for mantle hotspot impingement on continental crust (Pierce and Morgan, 1992; Hanan et al., 2008; Shervais and Hanan, 2008; Smith et al., 2009; Jean et al., 2014). The region contains a record of continuous bimodal volcanism extending over 17 Ma (Shervais and Hanan, 2008; Coble and Mahood, 2012; Henry et al., 2017) to the present, and documents the migration of time-transgressive rhyolitic volcanism from the Bruneau-Jarbidge volcanic center (circa 12 Ma) to its present location beneath the Yellowstone Plateau (Pierce and Morgan, 1992; Anders et al., 2009). Interaction between the mantle hotspot and overlying continental lithosphere has resulted in large rhyolite caldera-forming eruptions, followed by eruption of smaller basaltic shield volcanoes (Bonnichsen et al., 2008; Christiansen and McCurry, 2008; McCurry and Rodgers, 2009). Post-caldera basaltic flows form a veneer over the rhyolite ash flows and lavas and mask the complete volcanic record. Understanding the origin and evolution of the post-caldera basalts is a challenge because the lack of later uplift and erosion means that younger lava flows conceal older basalts. High-recovery continental scientific drilling is an effective method to address questions of geochemical and volcanic evolution through time, especially in relatively young volcanic provinces that lack exposure.

Project Hotspot drilled three deep boreholes in the Snake River Plain in order to provide a more complete understanding of the volcanic history of the SRP (Shervais et al., 2011, 2012, 2013). The 1,912 m deep Kimama borehole, located in the Axial Volcanic Zone of the Snake River Plain (Figure 1), recovered over 1,900 m of continuous core, including 1,803 m of basalt and 110 m of intercalated sediment (including sidetrack core; Potter, 2014). We present here a detailed petrologic and geochemical investigation of basalts from the Kimama core to determine the nature and extent of chemical changes through time at a fixed location, where physical and chemical characteristics of the crust and mantle lithosphere are relatively set. These data document long-term (5.5 Ma) petrogenetic processes common to intracontinental basalts associated with mantle hotspots and large igneous provinces.

FIGURE 1

Figure 1. Map of the Snake River Plain showing location of the Kimama drill site (KMA, yellow circle) in relation to inferred locations of Yellowstone-Snake River Plain silicic volcanic centers, the Sr 0.706 isopleth, Craters of the Moon (COM), a Pleistocene-Holocene locus of evolved magmatism, and the Great Rift, a source of Quaternary olivine tholeiite eruptions on the eastern SRP. Regionally significant drill core locations are shown in the central and eastern Snake River Plain: Mountain Home (MH, 1.3 km depth), Wendell-RASA (WR, 0.3 km depth), Kimberly (KMB, 2 km depth), INL-WO2 (WO2, 1.5 km depth) and Sugar City (SC, 0.7 km depth). Miocene volcanic centers in eastern Oregon, northern Nevada, and Idaho are also shown: High Rock volcanics (HRV), Hawk Valley (HV), Virgin Valley (VV), Castle Peak (CP), Dooley Mtn (DM), McDermitt (McD), Santa Rosa-Calico (SR-C), Silver City (SC), Juniper Mtn (JM), Owhyhee Humbolt (OH), Bruneau-Jarbidge (BJ), Jarbidge Rhyolite (JR) Twin Falls (TF), Picabo (P), Heise (H), and Yellowstone (Y). Figure modified from Shervais and Hanan (2008); location of Great Rift and Craters of the Moon from Hughes et al. (2002a).

Other deep boreholes on the SRP include the Sugar City borehole (0.7 km; Embree et al., 1978; Jean et al., in revision), the Idaho National Laboratory (INL) hole WO-2 (1.52 km; Shervais et al., 2006), and the Wendell-RASA borehole (0.3 km; Jean et al., 2013) (Figure 1). Geochemical and isotope analyses conducted by previous workers indicate that significant fractionation occurred at lower or mid-crustal depths in layered mafic magma reservoirs, and that interaction with continental lithosphere is the primary external influence on SRP basalt chemistry. The most important mechanism of magma differentiation is thought to be fractional crystallization accompanied by assimilation of genetically-related, previously-intruded mafic sills in mid-crustal magma chambers (Shervais et al., 2006; Jean et al., 2013). The range of primary magma compositions suggests the involvement of multiple, small magma batches (Leeman, 1982; Vetter and Shervais, 1992; Geist et al., 2002; Hughes et al., 2002a,b; Shervais et al., 2006; Jean et al., 2013). Shifts in the composition of primary magma sources through time and space have been documented by Vetter and Shervais (1992), Shervais et al. (2006), and Shervais and Vetter (2009). As the longest and most complete record of basalt volcanism and magma differentiation in the SRP, the Kimama drill core ties mafic volcanism to a transcrustal network of sills and sill complexes where magmas are processed and cycled to the surface.

Geological Background

Regional Setting

The central SRP is loosely defined as the portion of the SRP between the Owyhee Plateau, a highland in southwest Idaho, and the Great Rift, a north-northwest-trending fissure system that extends ~50 km southward from Craters of the Moon lava flow field to the Wapi shield volcano (Kuntz et al., 1982, 1992). Major rhyolitic volcanic fields of the central SRP include the 11-6 Ma Twin Falls eruptive center (Knott et al., 2016), and the 10.4-6.6 Ma Picabo eruptive center, for which the boundaries are poorly defined (Figure 1) (Bonnichsen et al., 2008; Drew et al., 2013). These rhyolitic centers are buried by younger basaltic lava flows. Beyond the SRP, to the north and south of the Kimama drill site, is the Miocene to recent Basin and Range Province.

During the late Pliocene through Pleistocene, the SRP was the locus of densely-spaced mafic volcanic centers along the axis of the YSRP hotspot track that erupted thick packages of basalt flows and formed the Axial Volcanic High (Hackett et al., 2004; Shervais et al., 2005). Mafic volcanism on the SRP began within 1-2 Ma of the cessation of YSRP silicic volcanism, and is primarily expressed by the eruption of monogenetic olivine tholeiite basalts (Hughes et al., 2002a). Although time-progressive basalt eruptions are evident at the inception of post-rhyolitic volcanism, Pliocene-Holocene basalt lavas on the SRP are distributed throughout the volcanic province and do not follow the progression of silicic volcanism to the NE (Hughes et al., 1999; Bonnichsen and Godchaux, 2002). Most SRP basalt volcanism is manifested as monogenetic, single-pulse lava fields, erupted as low volume (3–5 km³) flows from shields during short-duration (tens to hundreds of years) eruptions (Kuntz et al., 1992).

The unique style of SRP volcanism has been recognized as a product of small, mid-crustal magma chambers feeding eruptions from coalesced low-relief shield volcanoes, over relatively short durations. Volcanism is described as “plains-style” by Greeley (1982). “Plains-style” volcanism is similar to modern flow processes on the island of Hawaii and transitional between quiescent Hawaiian-style and the large volume flood-style volcanism typified by the Columbia River Basalt Group (Greeley, 1982). Vent constructs for SRP volcanoes are typically low due to the efficient transport of low-viscosity lava away from the vent in lava tubes. Eruptive centers often blend in with the surrounding topography because relatively little lava accumulates near the vent (Self et al., 1998). Between periods of volcanism, lava flows in low areas were mantled by loess and by lacustrine and fluvial sediments.

Snake River Plain Basalt Stratigraphy

The high effusion rate of basalts on the SRP favors emplacement via inflated pahoehoe flows, whereby lava travels through the molten core of the flow and breaks out of the flow front as flow lobes (Walker, 1991; Chitwood, 1994; Hon et al., 1994; Self et al., 1998). The transport of pahoehoe basalt lava over large distances is facilitated via lava tubes, tube complexes, or surface channelization by inflation processes (Self et al., 1998; Hughes et al., 1999). On the Snake River Plain, lava flows may extend as much as 50–60 km from the vent of origin (Shervais et al., 2005). Self et al. (1998) recognized that the inflation mechanism of pahoehoe produces lava flows that display similar geometries at variable spatial scales. In order of increasing scale, basalt lavas are emplaced as flow lobes (flow units), flows, and flow groups (Walker, 1991; Chitwood, 1994; Self et al., 1998).

Over the duration of a “plains-style” eruption, sheet flows and flow units from a single magma reservoir interlayer to form a complex aggregate of flows termed flow group (Hughes et al., 2002a,b; Welhan et al., 2002). Lava flow groups have thicknesses of < 1–106 m (flow groups 12 and 73, respectively). They are the two-dimensional equivalents of compound lava flow fields, such as the Wapi and Hell's Half Acre lava fields on the SRP, which have areal dimensions of kilometers to tens of kilometers. Each flow group or lava flow field comprises all of the volcanic activity from a monogenetic volcanic center over time scales of tens to hundreds of years (Greeley, 1982; Kuntz et al., 1992; Welhan et al., 2002; Champion, pers. commun. 2014). In core, flow groups are distinguished from one another by lithostratigraphic relationships, paleomagnetic polarity reversals or inclination changes, sediment interbeds, and by significant geochemical variation.

Monogenetic eruptive centers on the SRP are most likely fed by individual magma sources, as demonstrated by chemical variation between and within flow groups (Hughes et al., 2002b). However, in order to produce separate magma batches for every monogenetic center on the SRP, a stratified source region in which melts were produced over a range of depths and degrees of melting would be required (Hughes et al., 1997).

Methods

We selected 265 whole rock samples from the Kimama core for analysis, representing 74 of 78 identified basalt flow groups. Samples were preferentially selected from the massive interiors of lava flows to avoid oxidation and alteration. Major elements were analyzed by fused bead X-ray fluorescence spectrometry (XRF), and trace elements were analyzed by inductively coupled plasma mass spectrometry (ICP-MS).

One-inch diameter mini cores were extracted from the whole round cores and a portion of each plug was broken in two to three fragments using a rock hammer. Samples were crushed using a Gyral Grinder shatterbox with a tungsten carbide vessel, and then ground again with an agate mortar and pestle. Samples for major element analysis were ignited at 800°C for 24 h, after which 1 g of ignited sample was mixed with 5 g of a Claisse Li-borate flux and 6 drops of LiI (added as a releasing agent). Sample mixes were melted in Pt-Au metal crucibles at 1200°C in a muffle furnace, then poured into a heated Pt-Au metal disk mold and quenched into glass. Major element (SiO₂, TiO₂, Al₂O₃, MnO, Fe₂O₃, MgO, CaO, Na₂O, K₂O, P₂O₅ Cr₂O₃) were analyzed with a Philips 2400 X-Ray fluorescence (XRF) spectrometer at Utah State University or with a Rigaku ZSX Primus II XRF spectrometer at Brigham Young University.

The standard deviation for replicated values for USGS standard BCR-1 for XRF analyses conducted at Brigham Young University are SiO₂: 0.06%, TiO₂: 0.004%, Al₂O₃: 0.05%, Fe₂O₃: 0.06%, MnO: 0%, MgO: 0.02%, CaO: 0.01%, Na₂O: 0.01%, K₂O: 0.01%, and P₂O₅: 0%. The standard deviation for replicated values for USGS standard BHVO-1 for XRF analyses conducted at Utah State University are SiO₂: 0.12%, TiO₂: 0.03%, Al₂O₃: 0.09%, Fe₂O₃: 0.04%, MnO: 0%, MgO: 0.12%, CaO: 0.08%, Na₂O: 0.01%, K₂O: 0.01%, and P₂O₅: 0.01%. Samples were ignited to convert all Fe to Fe³⁺ for analyses. Loss on ignition (LOI) was performed for 184 samples to identify potential alteration. All tables and figures depict major element values normalized to 100% on a volatile free basis with Fe_total reported as Fe₂O₃. Fe_total as FeO* is also reported for convenience in Table 1 in Supplementary Material.

Trace-element concentrations were measured at Centenary College (Shreveport, LA) using a PerkinElmer 600 inductively coupled plasma-mass spectrometer (ICP-MS). Approximately 60 mg of each sample was dissolved in 2 mL HF and 3 mL HNO₃ for 3 h, with watch glasses preventing evaporation. Watch glasses were then removed and samples dried, after which another 3 mL of HNO₃ was added to the samples. The sample solution was left at 50°C overnight, and then dried at 90°C. A further addition of 3 mL of HNO₃ to the sample preceded immediate drying. Finally, the sample was brought into solution with 2–3 mL of 50% HNO₃, and brought to a total volume of 50 mL with 5% HNO₃. This procedure is modified from Jenner et al. (1990) and Neal (2001). Five milliliters of 10 ppb In, Rh, and Ru were added to the sample solution as internal standards to calibrate measured concentrations. Plasma lab software was used to map out sampling order and record measurements over the duration of the experiment. Major and trace element analyses made at Utah State University (XRF), Brigham Young University (XRF), and Centenary College (ICP-MS) are distinguished by symbols in Table 1 in Supplementary Material. To compare Kimama major and trace element analyses with compositions from regional SRP basalt lavas, we used published values from Kuntz et al. (1992) and Hughes et al. (2002b).

Results

Flow Groups and Flows in the Kimama Core

The Kimama area includes late Neogene to Quaternary basalts that were erupted from low-relief shield volcanoes, most of which are normal magnetic polarity lavas erupted during the (>781 ka) C1n Brunhes Normal Polarity Chron (Shervais et al., 2005). 21 paleomagnetic Chrons and subchrons were identified in the Kimama core (Potter, 2014). Basaltic lava flows overlie rhyolite in the Twin Falls and Picabo volcanic centers (Shervais et al., 2005, 2011, 2012, 2013; Knott et al., 2016). Rhyolite was not encountered in the Kimama drill core (Potter et al., 2011; Potter, 2014).

Potter (2014) identified 432 basalt flow units comprising 183 lava flows. In core, flows and flow groups are distinguished by lithostratigraphic relationships, paleomagnetic polarity reversals or inclination changes, sediment interbeds, and by significant geochemical variation. The lithostratigraphy, paleomagnetic characteristics, the paleomagnetic and Ar-Ar age model, and the accumulation rate of the Kimama drill core basalts are discussed in Potter (2014).

Using this stratigraphic framework, paleo-secular variations in magnetic stratigraphy, and geochemical indicators (e.g., FeO* = total iron as ferrous, TiO₂, K₂O, La/Lu), we recognize 78 distinct flow groups in the Kimama core, ranging from 0.274 to 105.6 m thick. (Figure 2, Table 2 in Supplementary Material). Flow groups 41 and 42, identified by paleomagnetic indicators, were too thin and rubbly to sample. Flow groups 57 and 75, identified by distinct stratigraphic and paleomagnetic indicators, were not sampled due to alteration. Based upon paleomagnetic and Ar-Ar data, as well as stratigraphic relationships, we document that this sequence represents ~5.5 million years of volcanism (from 6 Ma to 475 ka) (Potter, 2014).

FIGURE 2

Figure 2. Lithologic log showing stratigraphic locations of Kimama flow groups, numbered 1 through 78 from 13 m (43 ft) through 1,912 m (6,273 ft) depth. SROT basalt is represented by alternating gray and light gray layers. Low K SROT, high Fe-Ti, high K-Fe, and evolved flow groups are represented by green, blue, and red layers (respectively). A green gradient on gray layers demonstrates the location of low K alteration within SROT flow groups. Sediment interbeds of loess (orange) in the upper section of the drill core, and sandstone and siltstone (orange and yellow) are present in the lower depths of the drill core. Hyaloclastite (purple) is present at the base of the drill core.

Major Elements

The whole-rock major-and trace-element compositions of Kimama core samples (Table 1 in Supplementary Material), and variation diagrams (Figures 3, 4) reveal similarity to SROT lavas from the central and eastern SRP. Geochemistry displayed in stratigraphic context (Figure 5) demonstrates more variation. Kimama basalts have major-element compositional ranges of 43.2–50.4 wt. % SiO₂, 9.80–17.6 wt. % FeO*, 1.22–4.65 wt. % TiO₂, 5.00–11.0 wt. % MgO, 8.84–14.0 wt. % CaO, 11.5–15.8 wt. % Al₂O₃, 1.75–2.75 wt. % Na₂O, and 0.12–0.92 wt. % K₂O, 0.17–1.65 wt. % P₂O₅. In general, most Kimama SROT basalts document smooth increases of TiO₂, FeO*, P₂O₅, and K₂O and decreases of Al₂O₃, CaO, and Ni decreasing MgO (Figure 3).

FIGURE 3

Figure 3. Selected major and trace element variation diagrams showing Kimama compositional groups: group 1 (SROT samples; gray squares), group 2 (high Fe-Ti samples; blue squares), group 3 (high K-Fe samples; red triangles), evolved sample KA1B3901 (red star) and group 4, low K SROT samples (maroon diamonds). Dashed black lines in (A,B) indicate compositional thresholds for high Fe-Ti and low K SROT basalts: 0.11 wt% K₂O/TiO₂ for low K SROT lavas, and 3.6 wt% TiO₂ and 15 wt% FeO* for high Fe-Ti lavas. In (C), high K-Fe lavas have FeO > 17.5 wt% and K₂O > 0.65 wt%. The evolved lava (sample KA1B3901) has 1.91 wt% TiO₂, and 1.57 wt% K₂O.

FIGURE 4

Figure 4. Selected major and trace element variation diagrams with compositions for basalts from the Kimama drill core (colored symbols denote compositional type) compared to compositions of eastern Snake River Plain (ESRP) olivine tholeiites (crosses; Hughes et al., 2002b) and Craters of the Moon evolved lavas (circles; Kuntz et al., 1982). All diagrams show variation with respect to MgO wt%: (A), TiO₂ wt%; (B), FeO* wt%; (C), K₂O wt%; (D), SiO₂ wt%; (E), P₂O₅ wt%, and (F), Zr ppm.

FIGURE 5

Figure 5. Generalized stratigraphic column and selected chemical compositions of the Kimama drill core as a function of depth below the surface (in meters). We identify 78 flow groups and four compositional groups. Depths of SROT flows (gray squares) low K SROT flows (maroon diamonds), high Fe-Ti flows (blue squares), high K-Fe flows (red triangles), and the evolved sample (red diamond) are presented. Refer to Tables 1 and 2 in Supplementary Material for flow group compositional and stratigraphic details. Progressive up section fractional crystallization within flow groups are evident in upward-trending concentrations of FeO*, K₂O, TiO₂, and La/Lu. Recharge is evident as upward trending concentrations of MgO, P₂O₅, and Ni within flow groups.

Loss on ignition (LOI) is largely negative above 1055 m depth, with an average of −0.56 (range 0.34 to −2.24) wt% as a result of weight gain as FeO is oxidized to Fe₂O₃ during heating. Below 1,055 m depth, loss on ignition values are largely positive, with an average of 1.43 (range 9.41 to −0.83) wt%. The highest LOI (8.5–9.4 wt%) are found below 1,700 m depth, indicating extensive alteration by hydrothermal fluids.

These data reveal that the Kimama basalts define three geochemically-distinct groups: (1) Snake River Olivine Tholeiite (SROT), which includes most of the basalts from surface outcrops on the SRP, (2) tholeiitic basalts rich in iron and titanium (“Fe-Ti basalts”), and (3) a suite of rare high K₂O-FeO*-rich basalts similar to mafic lavas from the Craters of the Moon. In addition, there is a fourth group of low-K basalts that includes members of Group 1 basalts and is characterized by low K₂O (typically < 0.25 wt%) and K₂O/TiO2 ratios of ≤ 0.11 wt% (Figure 2).

Group 1 SROT dominate the sample set, with >90% of all analyzed samples from throughout the length of the drill core. They are similar in composition to ocean island basalts, and characterized by phenocrysts or glomerocrysts of olivine and plagioclase. Group 2 Fe-Ti basalts are characterized by high TiO₂ (3.6–4.5 wt%) and FeO* (15–18 wt%). They occur at five depth ranges: 343–359, 459–465, 522–548, 561–566, and 1,117–1,151 m depth. The Fe-Ti basalts fall on extensions of the SROT trends on element variation diagrams, and are inferred to be related to SROT by low-pressure fractionation. The Group 3 high K-Fe lavas are characterized by K₂O >0.65 wt% and 17.5–18.5 wt% FeO*, with distinctively high K₂O/TiO₂ ratios >0.5, and low MgO contents. They are found at only two depth ranges: near 318 m (flow group 12), 1,048 m (Flow group 49), and 1,077 m (flow group 51) (Figures 2, 5, Table 2 in Supplementary Material).

Group 4 includes 36 samples; all but one of these occur below 1,043 m depth. The low-K basalts appear to be normal SROT basalts that have lost K₂O in response to hydrothermal alteration. This is supported by the correlation of low-K basalts with high K₂O/TiO₂ ratios and high LOI (Figure 6, Table 1 in Supplementary Material). Alteration within the Kimama drill core is manifest as vesicle fillings at around 700 m depth, forming amygdules filled with calcite and quartz. By 950 m depth, amygdules filled with smectites and/or zeolites become common. Below 1,300 m, alteration becomes more pervasive, with iddingsitization of olivine phenocrysts and the alteration of interstitial glass to clay minerals (Sant, 2013).

FIGURE 6

Figure 6. Loss on Ignition (LOI in wt%) and K₂O/TiO₂ plotted against stratigraphic depth. (A): LOI shows greatest variability below ~1,050 m (3,444 ft) depth, with the highest LOI measurement (10.26 wt%) recorded at 1,905 m (6,247 ft) depth. Above ~1,050 m depth, measurements fall into a tight range between 0.34 and −1.27 wt% LOI. (B): The lowest K₂O/TiO₂ ratios (~0.12) are dominantly present in low K SROT samples below ~1,050 m depth, possibly indicating increased hydrothermal alteration and the removal of K₂O from SROT basalts. Fractional crystallization trends are visible as progressive, up section decreases in K₂O/TiO₂ in SROT samples between ~300 and 0 m depth.

Finally, there is one sample that cannot be easily fit into any of these groups, although it seems most comfortable in the high-K-Fe group: KA1B3901 (flow group 59). This sample is characterized by relatively high SiO₂ (53 wt%), high K₂O (1.57 wt%), and moderate MgO (6.21 wt%) (Table 1 in Supplementary Material).

Trace Elements

Trace element variations in the Kimama basalts generally mimic trends observed in correlative major elements. Thus, Zr, Nb, Y, and the REE correlate positively with FeO*, TiO₂ and P₂O₅, and Ba and Rb correlate with K₂O, whereas compatible elements such as Ni and Cr correlate positively with MgO.

Kimama basalts are modestly enriched in the light rare earth elements (LREE) relative to the heavy rare earth elements (HREE), with chondrite-normalized La/Lu = 3–8 and smooth patterns that lack Eu anomalies (or have very modest negative anomalies); they are generally similar to those observed in surface basalts of the eastern and central SRP (Figure 7A). This includes all SROT, Fe-Ti, and low-K SROT. Evolved high K-Fe basalts (Group 3) have similar slopes on chondrite-normalized plots but have higher concentrations, similar to or slightly higher than evolved basalts and trachybasalts from Craters of the Moon (Figure 7A).

FIGURE 7

Figure 7. (A) Rare earth-element (REE) plot of Kimama core basalts (blue lines), normalized to primitive mantle (McDonough and Sun, 1995) and (B) multi-element patterns for Snake River Plain (SRP) olivine tholeiites and Craters of the Moon evolved lavas are plotted for comparison (Kuntz et al., 1982; Hughes et al., 2002b). Trace elements are arranged in order of decreasing compatibility from right to left.

Multi-element (spider) diagrams document further similarities to published data for surface basalts and evolved Craters of the Moon-type lavas. Notable features include strong enrichments in Ba (similar to other basalts in the western USA), and depletions in Th, Sr and Y relative to primitive mantle values (Figure 7B).

Discussion

Chemical Suites and Stratigraphic Trends

Despite the overall chemical similarity in SRP Neogene basalts, flow groups in the Kimama drill core exhibit several compositional trends (Figure 2). Whole rock MgO, FeO*, TiO₂, P₂O₅, and K₂O (all wt%), plotted against stratigraphic depth isolate three basalt compositional types (Figure 4). Oxides such as Al₂O₃ and Na₂O vary without discernible trends, perhaps owing to the crystallization and flotation of plagioclase within the magma, however CaO (not shown) also varies systematically, but Al₂O₃ and Na₂O (also not shown) have no discernable trends.

SROT and high K-Fe flow groups are thought to represent unrelated magma batches, whereas the Fe-Ti flow groups probably represent evolved SROT magmas. In the following paragraphs, we discuss whether Fe-Ti, high K-Fe, and SROT basalts are compositionally related by similar petrogenetic processes, and the significance of low-K basalts below 1200 m depth. We also discuss the significance of the anomalously evolved sample KA1B3901 in flow group 59.

Out of 74 sampled flow groups, a total of 42 flow groups are classified as SROT based upon compositional ranges of 5.00–11.0 wt% MgO, 11.0–15.8 wt% FeO*, 0.21–0.92 wt% K₂O, and 1.76–3.63 wt% TiO₂. Flow groups 1–11, 13, 15–20, 22–24, 27, 30–40, 43, 44, 46, 47, 52, 58, 61, 64, and 70 display SROT chemical trends. SROT flows are found through the entire Kimama drill core, with the highest number of flows in the 16–1,200 m depth range. Seven flow groups are identified as high Fe-Ti lava flows based upon elevated concentrations of FeO* (13.8–17.6 wt%), and TiO₂ (2.67–4.65 wt%). High Fe-Ti flows are preferentially located in the upper 754 m of the drill core in flow groups 14, 21, 25, 26, 28, 54, and 55; two high Fe-Ti flow groups are present stratigraphically deeper at 1,119 and 1,138 m (flow groups 54 and 55, respectively). We identify 21 low-K lava flow groups (29, 45, 48, 50, 53, 57, 60, 62, 63, 65–69, 71–73, and 75–78) dominated by low K₂O/TiO₂ (≤0.11). Low-K SROT flows are concentrated from 1,200 to 1,912 m depth (Figure 2, Table 2 in Supplementary Material) and are discussed in the following section.

SROT flows below ~1,200 m depth are dominantly primitive, with low concentrations of FeO*, TiO₂, P₂O₅, and K₂O, and relatively high MgO, CaO, Cr, and Ni. The latter are less susceptible to alteration than K and are indicators of recharge processes. Many of these SROT flows are also low-K basalts, with abnormally low K₂O due to hydrothermal alteration. Nonetheless, the low-K SROT flows below 1,200 m depth are also low in FeO*, TiO₂, and P₂O₅, with high MgO, CaO, Cr, and Ni. Above 1,200 m depth, most SROT flows display cyclic variations in composition that are correlated with fractional crystallization and magma recharge, as discussed below.

SROT flows also exhibit a generalized increase of incompatible elements up section (e.g., K₂O and P₂O₅) that may reflect fractionation enrichment and/or the assimilation of previously emplaced ferrodioritic melts. Flow groups deeper in the drill core exhibit more primitive major and trace element concentrations (e.g., Figure 5). This trend may result from the addition of more enriched primitive magmas or progressively higher amounts of assimilation, as discussed below. Concentrations of REE and other incompatible elements also vary with depth, and substantiate recharge and fractionation cycles observed in the major element data (Figure 7).

Three flow groups were classified as high K-Fe lavas based upon anomalously high values of FeO* (≥17.8 wt%), K₂O (1.77 to 1.84 wt%), and TiO₂ (3.43–3.54 wt%), coupled with low MgO (3.40–3.94 wt%). Flow groups 12, 49, and 51 have compositions that are similar to those erupted within Craters of the Moon during the latest Pleistocene and Holocene. High K-Fe lavas are located at 318, 1,045, and 1,077 m depths, respectively (Table 2 in Supplementary Material). Sample KA1B3901 (flow group 59) has low FeO* (10.2 wt%) and TiO₂ (1.91 wt%) relative to the high K-Fe lavas, but nevertheless displays a similar evolved geochemical signature, including high SiO₂ (52.9 wt%), high Na₂O (2.70 wt%), and high K₂O (1.57 wt%). The members of the high K-Fe and evolved suites are the most chemically distinct flows in the Kimama drill core.

The REE patterns of SROT, low-K SROT, and Fe-Ti suites are broadly similar, implying a genetic connection. High K-Fe flow groups are 10x more enriched in both LREE and HREE concentrations than other Kimama chemical groups and fall within the Craters of the Moon compositional array (Figure 7).

Hydrothermal Alteration with Depth

Normal SRP lavas contain little to no water and are characterized by negative loss on ignition values, which reflects the conversion of FeO to Fe₂O₃ during ignition; this effect is especially noticeable because all SRP tholeiites have relatively high FeO/Fe₂O₃. Positive ignition loss reflects bound water in excess of that needed to offset the oxidation of ferrous iron. Since these basalts are basically anhydrous when fresh, this bound water represents hydrothermal alteration of groundmass glass to smectite, as documented by Sant (2013). Temperature logs from the Kimama bore hole record a geothermal gradient of 72–75 from about 980–1,440 m depth, with an average heat flow of 132 mW/m² (Lachmar et al., 2017). Plots of LOI vs. depth show that hydrothermally altered basalt is dominant below 1050 m depth, although the effects are variable and do not correlate in a simple fashion; only the deepest flows (>1,700 m) have consistent low K₂O and high LOI (Figure 6).

The effect of hydrothermal alteration on major element concentrations is seen most clearly in the K₂O/TiO₂ ratios: ratios > 0.11 follow normal igneous trends consistent with other SROT basalts (e.g., Hughes et al., 2002b). Samples with K₂O/TiO₂ ratios ≤ 0.11 plot below other SROT analyses. During normal differentiation of SROT basalts, K₂O and TiO₂ behave incompatibly. Since TiO₂ is generally immobile in hydrothermal fluids, the low K₂O/TiO₂ ratios must represent leaching of K₂O from the samples during the conversion of groundmass glass and mesostasis to smectite. On a plot of TiO₂ vs. K₂O, the low-K group clearly lies below the main field of SROT basalts, consistent with this interpretation (Figure 3C). All samples with K₂O/TiO₂ ratios ≤ 0.11 have positive LOI values, but not all samples with positive LOI have low K₂O/TiO₂ ratios.

A plot of K₂O/TiO₂ ratio vs. depth shows that the low-K samples all lie below 1,050 m depth, although many samples from >1,050 m depth plot on a trend consistent with the SROT at less than 1,050 m depth, suggesting that these samples still retain their primary signatures.

Fractionation/Enrichment and Recharge Cycles

The progressive enrichment of incompatible elements in stratigraphically upsection flow groups is commonly interpreted to represent ongoing eruptions from a fractionating magma chamber. Likewise, progressive depletion in incompatible elements, and concomitant enrichment of compatible elements upsection in a flow group, is interpreted to represent magma chamber recharge with primitive or parental melt compositions (Shervais et al., 2006). Upward fractionation cycles are indicated by a decrease in MgO (Cr, and Ni) and increases in FeO*, TiO₂, P₂O₅, and K₂O as a result of fractionation of Mg-rich olivine, Ca-Al-rich plagioclase, and Cr-spinel. Recharge cycles are indicated by increasing MgO and Ni, and decreases in FeO*, TiO₂, K₂O, and P₂O₅ (Figure 5).

Stratigraphically defined flow groups based on lithology, paleosecular magnetic variations, and sediment intercalations, as defined by Potter (2014), appear to correspond to magma fractionation or recharge cycles (Figure 5). However, flow groups 7, 9, 18, 20, 23, 48, 53, 54, 57, 58, 66, 68, 70, 75, and 78 show relatively constant compositions with depth, suggesting the emptying of a magma reservoir over relatively short time spans, with little or no coeval fractional crystallization. This is consistent with relatively high eruption rates that could empty a magma reservoir quickly.

Upward fractionation cycles are recognized in 21 flow groups in the Kimama drill core: flow groups 2, 5, 8, 10, 11, 13, 17, 19, 29, 33-37, 47, 58, 63, 64, 67, 72, and 73. Seven flow groups show brief intervals of upward fractionation superimposed on recharge trends (flow groups 8, 22, 23, 29, 65, 69, and 77). These short upward fractionation “steps” probably represent periods of quiescence during which neither eruptions nor magma recharge occur.

Other flow groups document progressive recharge of their magma chambers coeval with ongoing eruptions, such that lavas become progressively more primitive upsection, trending to low-K, high MgO compositions. This can be observed in six flow groups: 4, 16, 26, 27, 30, and 39. Flow groups 14, 38, 50, 52, and 60 also display brief intervals of recharge superimposed on the dominant fractionation trends.

The three high K-Fe flow groups and the evolved flow group (groups 12, 49, 51, and 59) are compositionally constant, but too thin to represent prolonged time intervals. Although all four sit atop underlying upward fractionation cycles, the large offset from REE patterns between SROT and high K-Fe or evolved flow groups suggests either a distinct parent magma or the assimilation of a crustal source, likely compositionally similar to Graveyard Point Intrusion gabbros or ferrodiorites (White, 2007). Therefore, connecting high K-Fe and evolved flows to underlying flow groups is problematic.

The occurrence of upward fractionation cycles and recharge cycles is consistent with the proposals of Shervais et al. (2006) and Brueseke et al. (2016) that magmas are processed through mid-crustal intrusions, in which individual sills form complex layers as the cumulate extract of crystal-melt fractionation. These layered mafic intrusions act as reactive filters which process the magma before it erupts. Individual sills may represent a single pulse of primitive magma which differentiates as it feeds a single monogenetic volcano on the surface.

Fractionation-Assimilation

Major processes that may control the evolution of continental basalts include fractional crystallization with no significant assimilation, fractional crystallization accompanied by assimilation of older crustal materials, and fractional crystallization accompanied by assimilation of previously intruded mafic magmas (ACMI-assimilation of consanguineous mafic intrusions; Shervais et al., 2006). These processes can be distinguished using plots of lithophile element ratios vs. a fractionation indicator such as Mg# (Shervais et al., 2006). In Figure 8 we plot Mg# (which decreases with fractional crystallization) against ratios of La/Lu and K₂O/P₂O₅. The ratio of La/Lu varies little during fractional crystallization of olivine and plagioclase, but will increase progressively in response to fractional crystallization-assimilation of either older continental crust or older mafic intrusions. In contrast, K₂O/P₂O₅ ratios will increase strongly with assimilation of older crustal materials, but decrease in response to assimilation of mafic intrusions. In Kimama SROT lavas, La/Lu ratios increase progressively as Mg# decreases, whereas K₂O/P₂O₅ ratios decrease progressively, showing that AFC involving older mafic intrusive rocks was the dominant process (Figure 8). The high K-Fe flow group displays the same trends of increasing La/Lu and decreasing K₂O/P₂O₅ ratios with decreasing MgO, showing that this group also must form by large degrees of fractional crystallization and assimilation of a gabbroic intrusion. In contrast, sample KA1B3901 (flow group 57) displays an increase in K₂O/P₂O₅ ratio with decreasing MgO, and may be a result of fractional crystallization with assimilation of continental crust (Figure 8A). The variation in La/Lu at high mg# in SROT implies a range of parental magma compositions formed either by different degrees of partial melting or by small variations in source composition.

FIGURE 8

Figure 8. Ratio plots of K₂O/P₂O₅ and La/Lu (chondrite normalized; McDonough and Sun, 1995) vs. Mg# (100*Mg/[Mg + Fe]). (A) Decreasing K₂O/P₂O₅ with decreasing Mg# is consistent with the assimilation of gabbroic host rock. (B) An increase in La/Lu with decreasing Mg# suggests the assimilation of a gabbroic component during fractional crystallization. Brown arrows show the expected fractional crystallization (FC) pathways, red arrows show the expected pathways of assimilation-fractional crystallization of continental crust, and green arrows show the expected pathways for assimilation and fractional crystallization of gabbro (AFC-gabbro).

Origin of Highly Evolved Flow Groups

High K-Fe lavas do not appear to be simply related to the parental basalts (Figures 3–5, 7). Variation diagrams of trace elements (Zr/Y-Nb/Y), and MgO variations demonstrate a lack of congruity, and elevated concentrations of REE and other incompatible elements suggest either a different magma source or a unique magmatic differentiation scenario. These lavas were generated in a similar fashion as Craters of the Moon lavas, via extreme fractional crystallization accompanied by assimilation (e.g., Whitaker et al., 2006, 2008; Putirka et al., 2009). However, the decrease in K₂O/P₂O₅ ratios (Figure 8) implies that older felsic crust was not involved forming in these flows (or Craters of the Moon), and that extreme fractional crystallization perhaps accompanied by assimilation of slightly older mafic sills was the dominant process.

Although flow group 59 (sample KA1B3901) has a similar major and trace element composition to Craters of the Moon evolved basalts, high K-Fe flows in the Kimama drill core have distinctly higher FeO, Zr, Sr, Sc, La, and lower Al₂O₃, at the same MgO compositions when compared with more “traditional” Craters of the Moon evolved lavas and may represent a different fractionation or assimilation process (Hughes et al., 2002b; Putirka et al., 2009).

The evolved and high K-Fe flow groups in the Kimama drill core may represent the distal portions of early Craters of the Moon lava flows that reached the Kimama site. The fact that these flows are thin is consistent with this idea. High K-Fe lavas range from 0.27 m (flow group 12) to 3.75 m (flow group 49) thick, and the evolved flow group (59) is 6.49 m thick. These thicknesses are well below the average flow group thickness of 23.6 m. However, the Kimama drill site is about 20 km from the exposed terminus of the exposed Craters of the Moon lava flows (Kuntz et al., 2007). This is less than half the maximum observed flow lengths in the SRP (50–60 km; Shervais et al., 2005), so long, thin flows may have reached the Kimama site. On the other hand, age projections from Potter (2014), suggest that high K-Fe flow groups 12, 49, and 51 (317.7–318.9, 1,045.0–1,048.8, and 1,077.1–1,078.5 m depths, and the evolved flow group 59 (1,185.0–1,191.5 m depth) erupted at ~1.0, ~3.3, ~3.4, and ~3.7 Ma (respectively), well beyond the 480 ka maximum recorded age of Craters of the Moon basalts (Putirka et al., 2009). Thus, either Craters of the Moon-type lavas erupted from other sources farther to the west, or magmatism at Craters of the Moon is much older than documented by surface flows, and the Kimama drill core samples the distal portions of early lava flows.

Melt Source Modeling

Chemical variations in parental basalts may be attributed either to differing degrees of partial melting, different depths of melting, or to different source compositions (e.g., Hughes et al., 2002b; Putirka et al., 2009; Shervais and Vetter, 2009). We have constructed a series of melt models to test these options, using three representative source compositions (primitive mantle, depleted MORB-source mantle, and enriched E-MORB source mantle. Each source region is modeled for a range of melt fractions (from 1 to 20%) using non-modal batch melting in two different depth regimes: shallow spinel-facies melting (<3 GPa or ~100 km depth) and deeper garnet-facies melting (>3 GPa or ~100 km depth). We compare the model results to five representative high-MgO (>9.28 wt%) basalts from the Kimama drill core on primitive mantle-normalized multi-element plots (Figure 9).

FIGURE 9

Figure 9. Multi-element patterns normalized to primitive mantle (McDonough and Sun, 1995) for Kimama core basalts. Partial melts from three source compositions are plotted for varying mineralogy (spinel lherzolite and garnet lherzolite) and percentages of melting. (A,B) Enriched mid ocean ridge basalt (E-MORB), (C,D) normal mid ocean ridge basalt (N-MORB), and (E,F) primitive mantle (PM) source compositions of spinel lherzolite and garnet lherzolite are used. We compare compositions of four primitive basalt samples, proxies for parent magmas, to determine the composition and melting conditions of the source for the Kimama drill core magmas. Trace elements are arranged in order of decreasing compatibility from right to left.

Partial melting of an N-MORB composition source in the spinel lherzolite facies results in depleted LREE concentrations (relative to HREE) in model melts. At extremely low melt fractions (less than 2%), HREE concentrations in the model melts are too high and LREE/HREE ratios too low to match observed primitive basalt compositions (Figure 9A). High field strength elements (HFSE) and K₂O also show suppressed values in the model melts. Within the garnet lherzolite facies, partial melting of an N-MORB composition source results in model melts that are depleted in LREE relative to HREE. An exception to this observation occurs at extremely low melt fractions (<2%), in which case HREE, K₂O, and HFSE concentrations in the model melts are too low to fit the data (Figure 9B).

When primitive mantle source compositions are melted in the spinel lherzolite facies (Figure 9C), the model melts generated are too low in LREE and LREE/HREE ratios. Partial melting of a primitive mantle composition in the garnet lherzolite facies produces model melts with LREE concentrations that are too low at large melt fractions and HREE concentrations that are too high at low melt fractions. At all but the lowest melt fractions, the model melts have HFSE concentrations that are too low to match SRP tholeiites (Figure 9D).

The best fit to the trace element patterns of the primitive Kimama basalts was for model melts generated from the partial melting of an E-MORB source in the spinel lherzolite facies (Figure 9E). Coherence is observed for all elements in the 7–15% melting range with the exception of Sr, which is consistently high in all of the model melts. Using the same source composition in a garnet lherzolite mode resulted in fits for the LREE within the ~10–20% melting range, but poor fits for the HREE (Figure 9F).

The depth of melting inferred from the trace element models (see also Jean et al., 2013, in revision) is also consistent with estimates using phase equilibria and silica geobarometry for Kimama basalts which give melt segregation depths between 80 and 110 km and within the spinel lherzolite facies (Bradshaw, 2012). These relatively low pressures imply that melting must occur within the sublithospheric conduit that has been imaged seismically (Schutt and Dueker, 2008; Stachnik et al., 2008; Obrebski et al., 2010) beneath the eastern Snake River Plain as inferred by Hanan et al. (2008).

Implications for Magma Evolution in Continental Volcanic Settings

Although SRP olivine tholeiites (SROT) are relatively homogenous, chemical variation between separate magmatic events (flow groups) is evident. Previous workers have demonstrated that chemical variation between SRP basalt flows is a result of fractional crystallization, crustal contamination, and partial melting occurring within the mid-crustal sill at pressures of ~0.6 GPa and temperatures of 1,205 ± 27°C (Kuntz et al., 1992; Shervais et al., 2006; Christiansen and McCurry, 2008; McCurry and Rodgers, 2009; Miller and Hughes, 2009; Putirka et al., 2009). For Kimama drill core basalts specifically, Bradshaw (2012) estimated pre-eruptive crystallization occurred at 0.2–0.5 GPa (7–17 km) and between 1,155 and 1,255°C. Putirka et al. (2009) argue for a three-stage process to explain the entire range of SRP lava compositions. For typical SRP olivine tholeiites (SROT), mantle-derived picrites ascend to the middle crust at depths of 20–10 km, where they undergo partial crystallization of olivine ± clinopyroxene. Storage of olivine tholeiite magmas in the middle crust (20–10 km) causes magma compositions to evolve to moderate MgO wt% (10%), at which point positive buoyancy is reached and migration through the middle crust occurs. The lack of clinopyroxene phenocrysts in SRP basalts requires that SRP magmas continued to evolve in shallow subvolcanic reservoirs prior to eruption, forming the low-pressure phenocryst assemblage olivine-plagioclase.

More evolved magmas, such as those associated with Craters of the Moon, require additional processing at depths of 15–0 km, where differentiation and resulting volatile content increases (1–2 wt% H₂O) causing the final eruption and ascent of magma through the middle and upper crust (e.g., Annen et al., 2006; Putirka et al., 2009).

The data presented here also document the cyclic nature of magma intrusion, fractional crystallization, and magma recharge, consistent with magma evolution in a series of stacked layered intrusions in the lower to middle crust, which has also been documented in other deep drill cores from the SRP (e.g., Shervais et al., 2006; Jean et al., 2013). These data support the SRP magma petrogenetic model of Shervais et al. (2006), in which magmas are shown to evolve through complex pathways of fractional crystallization, assimilation, and mixing at multiple crustal levels before eruption. A particular aspect of this model also supported here is the process referred to as “assimilation of consanguineous mafic intrusions” (ACMI; Shervais et al., 2006). This refers to the process in which the assimilant is not pre-existing continental crust (e.g., Shirley, 2013), but rather slightly older intrusions of genetically-related mafic magmas that form the layered mafic sill complex in the middle crust. This process is documented by the fractionation-related increase in LREE/HREE ratios accompanied by decreases in lithophile/high-field strength element ratios such as K₂O/P₂O₅ (Figure 8A).

Assimilation of consanguineaous mafic intrusions is facilitated by two processes. First, newly intruded magma is less dense than previously intruded sills that are now mostly crystallized. This means that new magma will tend to pond above older intrusions, and subsequent intrusions will continue to stack above older ones. Second, the newly intruded magmas will interact with more evolved portions of the older sills, which are typically located in the upper part of the crystallized sill. Overall, the evolved diorites of an older sill will have lower melting points than the sill, thereby facilitating assimilation.

In some cases, if the older sill is not completely crystallized, the freshly recharged magma will preferentially inject into the evolved residual magma (mush) of the older sill, mixing with the evolved residual magma (mush) to form a hybrid magma. This may result in wholesale replacement of the older magma mush, or may proceed gradually, resulting in progressively more primitive magma over time. Our data present evidence for both scenarios: in some cases, fractionation cycles succeed one another with no observed gradual recharge; in others, gradual recharge of the magma chamber takes place, as documented by the recharge cycles. These processes are observed in other deep core suites from the central and eastern SRP (Shervais et al., 2006; Jean et al., 2013).

The occurrence of recharge cycles in particular suggests that magma evolution in the middle crust takes place in relatively large (possibly km-scale?) layered intrusions, not 100-m scale sills (Shervais et al., 2006), and that layered mafic intrusions such as the Muskox (Irvine, 1970) may provide more robust analogies for this evolution than smaller sills like the Graveyard Point Intrusion (White, 2007). The continuous increase in concentrations of incompatible elements upsection in the drill core (e.g., La, Figure 5) is more compatible with longer-lived large scale intrusions than with many small, ephemeral intrusions, which are unlikely to result in continuous enrichment of the magma system. These sill-shaped layered intrusions are stacked in the upper middle crust by density contrasts with the underlying lower crust and overlying upper crust (Annen et al., 2015). Each subsequent intrusion will tend to pond above previous intrusions, which are denser than the newly intruded magma, or may tend to localize within the zone of residual melt of a previously intruded sill.

One consequence of this recharge-mixing-assimilation model is that successive magma bodies become progressively more enriched in incompatible elements over time. This is reflected in the progressive increase in K₂O, P₂O₅, and La/Lu upsection (Figure 5). This process is depicted schematically in Figure 10, which shows how mixing of newly recharged magma with residual melt (or assimilated fractional melt) from prior intrusions leads to enrichment of the mixed melt. Over time, successive mixtures become progressively enriched even though the recharge magma remains the same. Similar enrichments may also occur due to in situ crystallization in a large magma chamber (e.g., Langmuir, 1989).

FIGURE 10

Figure 10. In large mafic igneous provinces with high magma flux such as the SRP, pre-existing mafic magma intrusions are assimilated by genetically-related newer magma intrusions in a process we call “assimilation of consanguineous mafic intrusions” process (ACMI; Shervais et al., 2006). This conceptual diagram shows the time-progressive effects of ACMI. Ci and Cj are the concentrations of two different incompatible trace elements for which the bulk distribution coefficient (D) of C_i is less than that of C_j (e.g., D_ci <D_cj <1). The curved red arrows demonstrate assimilation and fractional crystallization (AFC) pathways that lead to progressively more evolved compositions and where the assimilant is solid intrusive rock of the same magma system. The blue dashed lines indicate recharge by more primitive magma. The mixed magma then experiences another cycle of evolution beginning with AFC. The compositional trend (black line) of Kimama basalts shows the “stair-step” effect of multiple cycles of AFC and recharge leading to more evolved compositions and echoing patterns visible in Figures 5, 6B.

The physical manifestation of our stacked sill model is depicted in Figure 11. Mantle-derived mafic magmas move upwards through the lower crust (not shown) and form large sill-like intrusions in the upper middle crust. The larger sill-like plutons (which form during episodes of high magma flux) evolve by crystal fractionation to form layered mafic intrusions (e.g., Irvine, 1970) that are periodically refreshed by new magma. Magma escaping from these layered plutons may erupt directly to the surface, or may be processed through small subvolcanic magma bodies at shallow depths (2–4 km) that are typically associated with a single volcano. As each pluton freezes, new sill-like intrusions pond above the older plutons to form a stacked sill complex. This process leads to assimilation of consanguineous mafic intrusions, as later intrusions cannibalize older ones and evolve by AFC processes that generally do not include pre-existing crustal rocks (e.g., Shervais et al., 2006).

FIGURE 11

Figure 11. Conceptual diagram of a layered mafic sill complex illustrating the process of “assimilation of consanguineous mafic intrusions” (ACMI). In this model, mantle-derived mafic magmas move upwards through the lower crust and form large sill-like plutons within the middle crust (10–20 km depth) during periods of high magma flux. The large sill-like plutons evolve through fractional crystallization and are periodically refreshed by newer magmas, eventually forming a layered mafic intrusion comprising cumulates of dunite, olivine gabbro, troctolite, and late-stage differentiates including ferrogabbro and ferrodiorite (e.g., Irvine, 1970). New sill-like intrusions pond above cooled sill-like intrusions to form a stacked sill complex. Within the stacked sill complex, new sills cannibalize older sills and undergo ACMI processes without the influence of pre-existing continental crust. Magmas may be transported to the surface through dikes, or they may be stalled and processed in small, subvolcanic intrusions at shallow depths (2–4 km).

We suggest that the physical and chemical connections that we observe in the Kimama drill core are common to intra-continental basalts and their crustal plutons, and may characterize mafic magma systems in continental crust, especially when magma flux is relatively high.

Conclusions

Geochemical data, along with previously-determined drill core stratigraphy and paleomagnetic data (Potter, 2014), show that basalts from the Kimama drill core on the axial high of the Snake River Plain vary between two main compositional arrays throughout 5.5 Ma of continuous eruption. Snake River olivine tholeiites (SROT) and their high Fe-Ti differentiates make up >99% of sampled flows. The remaining flows (<1%) comprise minor volumes of evolved high K-Fe lavas that share a compositional affinity to evolved flows erupted at Craters of the Moon.

The Kimama borehole samples lava flows presumably erupted from multiple shields in the region, but the similarity of mantle melting conditions, transport paths, or depths of evolution has resulted in lavas with generally similar compositions. The compositional variance within SROT and high Fe-Ti lavas observed in the Kimama drill core must reflect differing processes of petrogenesis from magmas of the same source. Low K flows below 1,050 m depth are correlated to increasing LOI, and we invoke secondary alteration of SROT lavas to explain these composition variants. Upward fractionation, or upsection increases in incompatible elements, K₂O and FeO* suggest fractional crystallization cycles as observed in layered mafic intrusions. Chemical reversals, or upsection increases in compatible elements and MgO concentrations, suggest episodes of progressive recharge of the system by more primitive melt.

We interpret the multiple chemical cycles evident in stratigraphic comparisons of Kimama drill core geochemistry to represent the fractionation of individual magma batches and the progressive recharge of crustal magma reservoirs, with each cycle representing eruptions from a nearby vent or vent system. Fractional crystallization is accompanied by assimilation, as shown by increases in La/Lu ratios with decreasing MgO, but the concomitant decrease in K₂O/P₂O₅ ratios shows that the assimilant is not pre-existing continental crust, but older mafic intrusions related to the continuing SROT volcanism. This is consistent with our FC-AFC models that use the Graveyard Point Intrusion diorite (White, 2007) as an analog for the mid-crustal sill complex. These fractionation and reversal trends provide evidence of a dynamic magma processing system over relatively short to long periods of time.

Our data show the importance of “assimilation of consanguineous mafic intrusions” (Shervais et al., 2006). In this model, large-volume mafic igneous provinces evolve by AFC processes in which the assimilant is dominantly older intrusions related to the same magma suite, not pre-existing continental crust. We suggest that model may be generally applicable to all mafic igneous provinces with high magma flux. This likely require large, km-scale layered intrusions in the middle to lower crust in order to produce the gradual replenishment trends seen throughout the drill core (Figure 11).

The stratigraphically thin (< 1.5 m) high K-Fe lavas found in the Kimama drill core are compositionally unrelated to SROT. We propose that high K-Fe flows erupted from Craters of the Moon and flowed southwest into the Kimama area, and that evolved magmas have been generated and episodically erupted from the Craters of the Moon region since at least 3.4 Ma.

Finally, we note that continental scientific drilling of volcanic provinces with >99% drill core recovery is a highly effective way to study both the overall chemical evolution of these provinces and their evolution through time (e.g., Shervais et al., 2014). It is particularly effective for understanding magma evolution in the crust and for inferring magma chamber processes in relatively young volcanic provinces.

Author Contributions

JS provided guidance during the preparation of the manuscript, specifically discussions of assimilation processes in the mafic mid-crustal sill complex of the Snake River Plain (central Idaho). JS oversaw the progress and completion on the dissertation that inspired this manuscript as my primary academic advisor at Utah State University (USU). JS also provided lab facilities and materials at USU where the majority of major element analyses on the Kimama drill core samples were conducted. EC provided guidance in the interpretation of major and trace element geochemical trends in Snake River Plain basalts, including identifying the relationship between some major element oxide percentages and loss on ignition (LOI) values. EC also oversaw the preparation and analysis of several Kimama drill core samples via X-ray fluorescence at Brigham Young University. SV provided lab facilities at Centenary College for the preparation of samples and the analysis of trace element concentrations via inductively coupled plasma mass spectrometry (ICPMS). KP logged and sampled the Kimama drill core while a Ph.D student at Utah State University. While a graduate student, KP prepared samples and conducted geochemical analyses, obtaining the data to identify compositional trends and make the larger-scale magma petrogenesis interpretations upon which this manuscript is based. The manuscript is based, in part, on KP Utah State University dissertation research (Potter, 2014), but later geochemical analyses were conducted by KP during her post-doc at Utah State University. The majority of the manuscript was written by KP with minor additions contributed by JS.

Conflict of Interest Statement

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Acknowledgments

This work was supported by DOE awards DE-EE0002848 DE-EE0006733, by the International Continental Drilling Program (ICDP), and by a consortium of universities, and is based upon the doctoral dissertation of Potter (2014). This dissertation is available online through the Utah State University library. We thank Jared Bryan and the BYU geochemistry lab for assistance, and for the helpful suggestions of reviewers. Discussions with Marlon Jean, Duane Champion, and the Hotspot Science Team (http://www.usu.edu/geo/shervais/Shervais-USU-Geology/Hotspot_Science_Team.html) were especially helpful, but any errors are our own.

Supplementary Material

The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2018.00010/full#supplementary-material

References

Anders, M. H., Saltzman, J., and Hemming, S. R. (2009). Neogene tephra correlations in eastern Idaho and Wyoming for Yellowstone hotspot-related volcanism and tectonic activity. Geol. Soc. Am. Bull. 121, 837–856. doi: 10.1130/B26300.1

CrossRef Full Text | Google Scholar

Annen, C., and Sparks, R. S. J. (2002). Effects of repetitive emplacement of basaltic intrusions on thermal evolution and melt generation in the crust. Earth Planet. Sci. Lett. 203, 937–955. doi: 10.1016/S0012-821X(02)00929-9

CrossRef Full Text | Google Scholar

Annen, C., Blundy, J. D., and Sparks, R. S. J. (2006). The genesis of intermediate and silicic magmas in deep crustal hot zones. J. Petrol. 47/3, 505–539. doi: 10.1093/petrology/egi084

CrossRef Full Text | Google Scholar

Annen, C., Blundy, J. D., Leuthold, J., and Sparks, R. S. J. (2015). Construction and evolution of igneous bodies. towards an integrated perspective of crustal magmatism. Lithos 230, 206–221. doi: 10.1016/j.lithos.2015.05.008

CrossRef Full Text | Google Scholar

Bachmann, O., Miller, C. F., and Silva, S. (2007). The volcanic–plutonic connection as a stage for understanding crustal magmatism. J. Volcanol. Geotherm. Res. 167, 1–23. doi: 10.1016/j.jvolgeores.2007.08.002

CrossRef Full Text | Google Scholar

Bonnichsen, B., and Godchaux, M. M. (2002). “Late Miocene, Pliocene, and Pleistocene geology of southwestern Idaho with emphasis on basalts in the Bruneau-Jarbidge, Twin Falls, and western Snake River Plain regions,” in Tectonic and Magmatic Evolution of the Snake River Plain Volcanic Province, Vol. 30, Idaho Geological Survey Bulletin (Idaho Geological Survey Press), 233–312.

Bonnichsen, B., Leeman, W. P., Honjo, N., McIntosh, W. C., and Godchaux, M. M. (2008). Miocene silicic volcanism in southwestern Idaho: geochronology, geochemistry, and evolution of the central Snake River Plain. Bull. Volcanol. 70, 315–342. doi: 10.1007/s00445-007-0141-6

CrossRef Full Text | Google Scholar

Bradshaw, R. W. (2012). Mineral Chemistry of Basalts Recovered from Hotspot Snake River Scientific Drilling Project, Idaho: Source and Crystallization Characteristics. Master's thesis, Brigham Young University, Provo.

Google Scholar

Brueseke, M. E., Hobbs, J. M., Bulen, C. L., Mertzman, S. A., Puckett, R. E., Walker, J. D., et al. (2016). Cambrian intermediate-mafic magmatism along the laurentian margin: evidence for flood basalt volcanism from well cuttings in the southern Oklahoma Aulacogen (U.S.A.). Lithos 260, 164–177. doi: 10.1016/j.lithos.2016.05.016

CrossRef Full Text | Google Scholar

Cashman, K. V., Sparks, R. S., and Blundy, J. D. (2017). Vertically extensive and unstable magmatic systems: a unified view of igneous processes. Science 355:eaag3055. doi: 10.1126/science.aag3055

PubMed Abstract | CrossRef Full Text | Google Scholar

Chitwood, L. A. (1994). Inflated basaltic lava: examples of processes and landforms from central and southeast Oregon. Or. Geol. 56, 11–21.

Christiansen, E. H., and McCurry, M. (2008). Contrasting origins of cenozoic silicic volcanic rocks from the western cordillera of the United States. Bull. Volcanol. 70, 251–267. doi: 10.1007/s00445-007-0138-1

CrossRef Full Text | Google Scholar

Coble, M. A., and Mahood, M. A. (2012). Initial impingement of the Yellowstone plume located by widespread silicic volcanism contemporaneous with Columbia River flood basalts. Geology 40, 655–665. doi: 10.1130/G32692.1

CrossRef Full Text | Google Scholar

Drew, D. L., Bindeman, I. N., Watts, K. E., Schmitt, A. K., Fu, B., and McCurry, M. (2013). Crustal-scale recycling in caldera complexes and rift zones along the Yellowstone hotspot track: O and Hf isotopic evidence in diverse zircons from voluminous rhyolites of the Picabo volcanic field, Idaho. Earth Planet. Sci. Lett. 381, 63–77. doi: 10.1016/j.epsl.2013.08.007

CrossRef Full Text | Google Scholar

Embree, G. F., Lovell, M. D., and Doherty, D. J. (1978). Drilling Data from Sugar City Exploration Well, Madison County, Idaho. U.S. Geological Survey Open File Report 78-1095.

Geist, D. J., Sims, E. N., Hughes, S. S., and McCurry, M. (2002). Open-system evolution of a single episode of Snake River Plain magmatism, in Link, P. K., and Mink, L. L., eds., Geology, hydrogeology, and environmental remediation, Idaho National Engineering and Environmental Laboratory, eastern Snake River Plain, Idaho. Geol. Soc. Am. 353, 193–204. doi: 10.1130/SPE353

CrossRef Full Text | Google Scholar

Greeley, R. (1982). The Snake River Plain, Idaho: representative of a new category of volcanism. J. Geophys. Res. 87, 2705–2712. doi: 10.1029/JB087iB04p02705

CrossRef Full Text | Google Scholar

Hackett, W. R., Smith, R. P., and Khericha, S. (2004). Volcanic hazards of the Idaho National Engineering and Environmental Laboratory, southeast Idaho, in B. Bonnichsen, C.M. White, and M. McCurry, eds., Tectonic and magmatic evolution of the Snake River Plain Volcanic Province. Idaho Geol. Survey Bull. 30, 461–482.

Google Scholar

Hanan, B. B., Shervais, J., and Vetter, S. (2008). Yellowstone plume-continental lithosphere interaction beneath the Snake River Plain. Geology 36, 51–54. doi: 10.1130/G23935A.1

CrossRef Full Text

Henry, C. D., Castor, S. B., Starkel, W. A., Ellis, B. S., Wolff, J. A., Laravie, J. A., et al. (2017). Geology and evolution of the McDermitt caldera, northern Nevada and southeastern Oregon, western USA. Geosphere 13, 1066–1112. doi: 10.1130/GES01454.1

CrossRef Full Text | Google Scholar

Hon, K., Kauahikaua, J., Denlinger, R., and Mackay, K. (1994). Emplacement and inflation of pahoehoe sheet flows: observations and measurements of active lava flows on Kilauea Volcano, Hawaii. Geol. Soc. Am. Bull. 106, 351–370. doi: 10.1130/0016-7606(1994)106<0351:EAIOPS>2.3.CO;2

CrossRef Full Text | Google Scholar

Hughes, S. S., McCurry, M., and Geist, D. J. (2002b). Geochemical correlations and implications for the magmatic evolution of basalt flow groups at the Idaho National Engineering and Environmental Laboratory, in Link, P.K., and Mink, L.L., eds., geology, hydrogeology, and environmental remediation: Idaho National Engineering and Environmental Laboratory, eastern Snake River Plain, Idaho. Geol. Soc. Am. Special Pap. 353, 151–173. doi: 10.1130/0-8137-2353-1.151

CrossRef Full Text | Google Scholar

Hughes, S. S., Wetmore, P. H., and Casper, J. L. (2002a). “Evolution of Quaternary tholeiitic basalt eruptive centers on the eastern Snake River Plain, Idaho,” in Tectonic and Magmatic Evolution of the Snake River Plain Volcanic Province, Vol. 30, Idaho Geological Survey Bulletin, eds B. Bonnichsen, C. M. White, and M. McCurry (Idaho Geological Survey Press), 363–385.

Google Scholar

Hughes, S. S., Smith, R. P., Hackett, W. R., and Anderson, S. R. (1999). “Mafic volcanism and environmental geology of the eastern Snake River Plain, Idaho,” in Guidebook to the Geology of Eastern Idaho (Pocatello, ID: Idaho Museum of Natural History), 143–168.

Google Scholar

Hughes, S., Wetmore, P., and Casper, J. (1997). Geochemical interpretation of basalt stratigraphy and Quaternary mafic volcanism, eastern Snake River Plain, Idaho. Geol. Soc. Am. Abstracts Prog. 29, A-298.

Irvine, T. N. (1970). “Crystallization sequences in the Muskox intrusion and other layered intrusions,” in Symposium on the Bushveld Igneous Complex and Other Layered Intrusions, Vol. 1 (Pretoria: Geological Society of South Africa Special Publication), 441–476.

Jean, M. M., Hanan, B. B., and Shervais, J. W. (2014). Yellowstone Hotspot – continental lithosphere interaction. Earth Planet. Sci. Lett. 389, 119–131. doi: 10.1016/j.epsl.2013.12.012

CrossRef Full Text | Google Scholar

Jean, M. M., Shervais, J. W., Champion, D. E., and Vetter, S. K. (2013). Geochemical and paleomagnetic variations in basalts from the Wendell Regional Aquifer Systems Analysis (RASA) drill core: evidence for magma recharge and assimilation–fractional crystallization from the central Snake River Plain, Idaho. Geosphere 9, 1319–1335. doi: 10.1130/GES00914.1

CrossRef Full Text | Google Scholar

Jenner, G. A., Longerich, H. P., Jackson, S. E., and Fryer, B. J. (1990). ICP–MS—A powerful tool for high- precision trace-element analysis in Earth science: evidence from analysis of selected U.S.G.S. reference samples. Chem. Geol. 83, 133–148. doi: 10.1016/0009-2541(90)90145-W

CrossRef Full Text | Google Scholar

Knott, T. R., Reichow, M. K., Branney, M. J., Finn, D. R., Coe, R. S., Storey, M., et al. (2016). Rheomorphic ignimbrites of the Rogerson Formation, central Snake River plain, USA: record of mid-Miocene rhyolitic explosive eruptions and associated crustal subsidence along the Yellowstone hotspot track. Bull. Volcanol. 78:23. doi: 10.1007/s00445-016-1003-x

CrossRef Full Text | Google Scholar

Kuntz, M., Champion, D., Spiker, E., Lefebvre, R., Covington, H., and McBroome, L. (1982). The Great Rift and the evolution of the Craters of the Moon lava field, Idaho, in Bill Bonnichsen and R.M. Breckenridge, eds., Cenozoic Geology of Idaho. Idaho Bureau Mines Geol. Bull. 26, 423–438.

Google Scholar

Kuntz, M., Covington, H., and Schorr, L. (1992). An overview of basaltic volcanism of the eastern Snake River Plain, Idaho, in P.K. Link, M.A. Kuntz, and L.P. Platt, eds., regional geology of eastern Idaho and western Wyoming. Geol. Soc. Am. Memoir 179, 227–267. doi: 10.1130/MEM179-p227

CrossRef Full Text | Google Scholar

Kuntz, M. A., Skipp, B., Champion, D. E., Gans, P. B., Van Sistine, D. P., and Snyders, S. R. (2007). Geologic Map of the Craters of the Moon 30' x 60' quadrangle, Idaho. U.S. Geological Survey Scientific Investigations Map 2969, 64-p. pamphlet, 1 plate, scale 1:100,000 (Washington, DC).

Google Scholar

Lachmar, T. E., Freeman, T. G., Sant, C. J., Walker, J. R., and Blackwell, D. D. (2017). Effect of an 860-m thick, cold, freshwater aquifer on geothermal potential along the axis of the eastern Snake River Plain, Idaho. Geotherm. Energy 5:16. doi: 10.1186/s40517-017-0086-8

CrossRef Full Text | Google Scholar

Langmuir, C. (1989). Geochemical consequences of In situ crystallization. Nature 340, 199–205. doi: 10.1038/340199a0

CrossRef Full Text | Google Scholar

Leeman, W. P. (1982). Olivine tholeiitic basalts of the Snake River Plain, Idaho, in Bill Bonnichsen and R.M. Breckenridge, eds., Cenozoic Geology of Idaho. Idaho. Bureau Mines Geol. Bull. 26, 181–191.

Lipman, P. W. (1984). The roots of ash-flow calderas in western North America: windows into the tops of granitic batholiths. J. Geophys. Res. 89, 8801–8841. doi: 10.1029/JB089iB10p08801

CrossRef Full Text | Google Scholar

McCurry, M., and Rodgers, D. W. (2009). Mass transfer along the Yellowstone hotspot track I: petrologic constraints on the volume of mantle-derived magma. J. Volcanol. Geotherm. Res. 188, 86–98. doi: 10.1016/j.jvolgeores.2009.04.001

CrossRef Full Text | Google Scholar

McDonough, W. F., and Sun, S. S. (1995). The composition of the Earth. Chem. Geol. 120, 223–253. doi: 10.1016/0009-2541(94)00140-4

CrossRef Full Text | Google Scholar

Metcalf, R. V. (2004). Volcanic–plutonic links, plutons as magma chambers and crust–mantle interaction: A lithospheric scale view of magma systems. Earth Environ. Sci. Trans. R. Soc. Edinb. 95, 357–374. doi: 10.1017/S0263593300001127

CrossRef Full Text | Google Scholar

Miller, M., and Hughes, S. (2009). Mixing primitive and evolved olivine tholeiite magmas in the eastern Snake River Plain, Idaho. J. Volcanol. Geotherm. Res. 188, 153–161. doi: 10.1016/j.jvolgeores.2009.06.004

CrossRef Full Text | Google Scholar

Neal, C. R. (2001). The interior of the Moon: The presence of garnet in the primitive, deep lunar mantle. J. Geophys. Res. 106, 27865–27885. doi: 10.1029/2000JE001386

CrossRef Full Text | Google Scholar

Obrebski, M., Allen, M. R., Xue, M., and Hung, S.-H. (2010). Slab-plume interaction beneath the Pacific Northwest. Geophys. Res. Lett. 37:L14305. doi: 10.1029/2010GL043489

CrossRef Full Text | Google Scholar

Pierce, K. L., and Morgan, L. A. (1992). “The track of the Yellowstone hotspot: volcanism, faulting, and uplift,” in Regional Geology of Eastern Idaho and Western Wyoming, Vol. 179, eds P. K. Link, M. A. Kuntz, and L. B. Platt (Boulder, CO: Geological Society of America Memoir), 1–54. doi: 10.1130/MEM179-p1

CrossRef Full Text

Potter, K. E. (2014). The Kimama Core: A 6.4 Ma Record of Volcanism, Sedimentation, and Magma Petrogenesis on the Axial Volcanic High, Snake River Plain. I. D. Dissertation. Utah State University, Logan.

Google Scholar

Potter, K. E., Bradshaw, R., Sant, C. J., King, J., Shervais, J. W., and Christiansen, E. J. (2011). Project hotspot: insight into the subsurface stratigraphy and geothermal potential of the Snake River Plain. Geotherm. Resourc. Council Transac. 35, 967–971.

Putirka, K. D., Kuntz, M. A., Unruh, D. M., and Vaid, N. (2009). Magma evolution and ascent at the Craters of the Moon and neighboring volcanic fields, Southern Idaho, USA: implications for the evolution of polygenetic and monogenetic volcanic fields. J. Petrol. 50, 1639–1665. doi: 10.1093/petrology/egp045

CrossRef Full Text | Google Scholar

Sant, C. (2013). Geothermal Alteration of Basaltic Core from the Snake River Plain, Idaho. Master's thesis. Utah State University, Logan.

Google Scholar

Schutt and Dueker (2008). Crust and upper mantle velocity structure of the Yellowstone hotspot and surroundings. J. Geophys. Res. 113:B03320. doi: 10.1029/2007JB005109

CrossRef Full Text

Self, S., Keszthelyi, L., and Thordarson, T. (1998). The importance of pahoehoe. Annu. Rev. Earth Planet. Sci. 26, 81–110. doi: 10.1146/annurev.earth.26.1.81

CrossRef Full Text | Google Scholar

Shervais, J. W., and Hanan, B. B. (2008). Lithospheric topography, tilted plumes, and the track of the Snake River–Yellowstone hotspot. Tectonics 27:5 doi: 10.1029/2007TC002181

CrossRef Full Text | Google Scholar

Shervais, J. W., and Vetter, S. K. (2009). High-K alkali basalts of the western Snake River Plain (Idaho): abrupt transition from tholeiitic to mildly alkaline plume-derived basalts. J. Volcanol. Geotherm. Res. 188, 141–152. doi: 10.1016/j.jvolgeores.2009.01.023

CrossRef Full Text | Google Scholar

Shervais, J. W., Arndt, N., and Goodenough, K. M. (2014). Drilling the solid earth: global geodynamic cycles and earth evolution. Int. J. Earth Sci. 95, 85–92. doi: 10.1007/s00531-014-1073-y

CrossRef Full Text | Google Scholar

Shervais, J. W., Evans, J. P., Christiansen, E. H., Schmitt, D. R., Kessler, J. A., Potter, K. E., et al. (2011). Project hotspot: the Snake River scientific drilling project. Geotherm. Resourc. Council Transac. 35, 995–1003.

Shervais, J. W., Kauffman, J. D., Gillerman, V. S., Othberg, K. L., Vetter, S. K., Hobson, V. R., et al. (2005). Basaltic volcanism of the central and western Snake River Plain: a guide to field relations between Twin Falls and Mountain Home, Idaho. Field Guides 6, 27–52. doi: 10.1130/2005.fld006(02)

CrossRef Full Text | Google Scholar

Shervais, J. W., Nielson, D. L., Evans, J. P., Christensen, E. J., Morgan, L., Shanks, W. C., et al. (2012). Hotspot: the Snake River geothermal drilling project – initial report. Geotherm. Resourc. Council Transac. 36, 767–772.

Google Scholar

Shervais, J. W., Schmidt, D. R., Nielson, D., Evans, J. P., Christiansen, E. H., Morgan, L., et al. (2013). First results from HOTSPOT: the Snake River Plain scientific drilling project, Idaho, U.S.A. Sci. Drilling 15, 36–45. doi: 10.5194/sd-15-36-2013

CrossRef Full Text | Google Scholar

Shervais, J. W., Vetter, S. K., and Hanan, B. B. (2006). Layered mafic sill complex beneath the eastern Snake River Plain: evidence from cyclic geochemical variations in basalt. Geology 34, 365– 368. doi: 10.1130/G22226.1

CrossRef Full Text | Google Scholar

Shirley, E. K. (2013). A Precambrian history of cratonic North American crust beneath the Snake River Plain, Idaho. Master's thesis. Boise State University, Boise, ID.

Google Scholar

Smith, R. B., Jordan, M., Steinberger, B., Puskas, C., Farrell, J., Waite, G. P., et al. (2009). Geodynamics of the Yellowstone hotspot and mantle plume: seismic and GPS imaging, kinematics, and mantle flow. J. Volcanol. Geotherm. Res. 188, 26–56 doi: 10.1016/j.jvolgeores.2009.08.020

CrossRef Full Text | Google Scholar

Stachnik, J. C., Dueker, K., Schutt, D. L., and Yuan, H. (2008). Imaging Yellowstone plume– lithosphere interactions from inversion of ballistic and diffusive Rayleigh wave dispersion and crustal thickness data. Geochem. Geophys. Geosyst. 9:Q06004. doi: 10.1029/2008GC001992

CrossRef Full Text | Google Scholar

Vetter, S. K., and Shervais, J. W. (1992). Continental basalts of the Boise River Group near Smith Prairie, Idaho. J. Geophys. Res. B Solid Earth Planets 97, 9043–9061. doi: 10.1029/92JB00209

CrossRef Full Text | Google Scholar

Walker, G. P. L. (1991). Structure, and origin by injection under surface crust, of tumuli, “lava rises,” “lava-rise pits,” and “lava inflation clefts” in Hawaii. Bull. Volcanol. 53, 546–558. doi: 10.1007/BF00298155

CrossRef Full Text | Google Scholar

Welhan, J. A., Johannesen, C. M., Reeves, K. S., Clemo, T. M., Glover, J. A., and Bosworth, K. W. (2002). Morphology of inflated pahoehoe lavas and spatial architecture of their porous and permeable zones, eastern Snake River Plain, Idaho. Geol. Soc. Am. Special Pap. 353, 135–150. doi: 10.1130/0-8137-2353-1.135

CrossRef Full Text | Google Scholar

Whitaker, M. L., Nekvasil, H., Lindsley, D. H., and Difrancesco, N. J. (2006). The role of pressure in producing compositional diversity in intraplate basaltic magmas. J. Petrol. 48, 365–393. doi: 10.1093/petrology/egl063

CrossRef Full Text | Google Scholar

Whitaker, M. L., Nekvasil, H., Lindsley, D. H., and McCurry, M. (2008). Can crystallization of olivine tholeiite give rise to potassic rhyolites? —an experimental investigation. Bull. Volcanol. 70, 417–434. doi: 10.1007/s00445-007-0146-1

CrossRef Full Text | Google Scholar

White, C. M. (2007). The Graveyard Point Intrusion: an example of extreme differentiation of Snake River Plain basalt in a shallow crustal pluton. J. Petrol. 48, 303–325. doi: 10.1093/petrology/egl062

CrossRef Full Text | Google Scholar