Open Collections

UBC Faculty Research and Publications

Wrangellia flood basalts in Alaska: A record of plume-lithosphere interaction in a Late Triassic accreted.. Greene, Andrew R. 2011

You don't seem to have a PDF reader installed, try download the pdf

Item Metadata

Download

Media
Weis_AGU_2008GC002092.pdf
Weis_AGU_2008GC002092.pdf [ 2.73MB ]
Metadata
JSON: 1.0075971.json
JSON-LD: 1.0075971+ld.json
RDF/XML (Pretty): 1.0075971.xml
RDF/JSON: 1.0075971+rdf.json
Turtle: 1.0075971+rdf-turtle.txt
N-Triples: 1.0075971+rdf-ntriples.txt
Citation
1.0075971.ris

Full Text

Wrangellia flood basalts in Alaska: A record of plume-lithosphere interaction in a Late Triassic accreted oceanic plateau Andrew R. Greene, James S. Scoates, and Dominique Weis Pacific Centre for Isotopic and Geochemical Research, Department of Earth and Ocean Sciences, University of British Columbia, 6339 Stores Road, Vancouver, British Columbia V6T 1Z4, Canada (agreene@eos.ubc.ca) [1] The Wrangellia flood basalts are part of one of the best exposed accreted oceanic plateaus on Earth. They provide important constraints on the construction of these vast submarine edifices and the source and temporal evolution of magmas for a plume head impinging beneath oceanic lithosphere. Wrangellia flood basalts (231–225 Ma) extend 450 km across southern Alaska (Wrangell Mountains and Alaska Range) where 3.5 km of mostly subaerial flows are bounded by late Paleozoic arc volcanics and Late Triassic limestone. The vast majority of the flood basalts are light rare earth element (LREE) -enriched high-Ti basalt (1.6–2.4 wt % TiO2) with uniform ocean island basalt (OIB) -type Pacific mantle isotopic compositions (eHf(t) = +9.7 to +10.7; eNd(t) = +6.0 to +8.1; t = 230 Ma). However, the lowest 400 m of stratigraphy in the Alaska Range is LREE-depleted low-Ti basalt (0.4–1.2 wt % TiO2) with pronounced negative high field strength element (HFSE) anomalies and Hf isotopic compositions (eHf(t) = +13.7 to +18.4) that are decoupled from Nd (eNd(t) = +4.6 to +5.4) and displaced well above the OIB mantle array (DeHf = +4 to +8). The radiogenic Hf of the low-Ti basalts indicates involvement of a component that evolved with high Lu/Hf over time but not with a correspondingly high Sm/Nd. The radiogenic Hf and HFSE-depleted signature of the low-Ti basalts suggest pre-existing arc lithosphere was involved in the formation of flood basalts that erupted early in construction of part of the Wrangellia plateau in Alaska. Thermal and mechanical erosion of the base of the lithosphere by the impinging plume head may have led to melting of arc lithosphere or interaction of plume-derived melts and subduction-modified mantle. The high-Ti lavas dominate the main phase of construction of the plateau and were derived from a depleted mantle source distinct from the source of MORB and with compositional similarities to that of ocean islands (e.g., Hawaii) and plateaus (e.g., Ontong Java) in the Pacific Ocean. Components: 18,987 words, 18 figures, 4 tables. Keywords: Wrangellia; Nikolai Formation; Alaska; oceanic plateau; high-titanium basalt; low-titanium basalt. Index Terms: 1033 Geochemistry: Intra-plate processes (3615, 8415); 1037 Geochemistry: Magma genesis and partial melting (3619); 1040 Geochemistry: Radiogenic isotope geochemistry. Received 11 May 2008; Revised 23 September 2008; Accepted 3 October 2008; Published 4 December 2008. Greene, A. R., J. S. Scoates, andD.Weis (2008),Wrangellia flood basalts inAlaska: A record of plume-lithosphere interaction in a Late Triassic accreted oceanic plateau, Geochem. Geophys. Geosyst., 9, Q12004, doi:10.1029/2008GC002092. G3GeochemistryGeophysicsGeosystems Published by AGU and the Geochemical Society AN ELECTRONIC JOURNAL OF THE EARTH SCIENCES Article Volume 9, Number 12 4 December 2008 Q12004, doi:10.1029/2008GC002092 ISSN: 1525-2027 Copyright 2008 by the American Geophysical Union 1 of 34 1. Introduction [2] Oceanic plateaus and continental flood basalts (CFBs) represent transient large igneous provinces (LIPs) that are produced from the largest mantle melting events recorded on Earth. Oceanic plateaus and CFBs form from unusually high magmatic fluxes during emplacement over several million years or less [Saunders, 2005]. A longstanding controversy concerning the origin of magmas in many transient LIPs worldwide is whether they form by melting of the lithospheric mantle during any stage of LIP emplacement. CFBs have com- positions that indicate involvement of subconti- nental lithospheric mantle [e.g., Peate and Hawkesworth, 1996]. Compositional evidence of involvement of the lithospheric mantle in lavas erupted in oceanic plateaus, however, remains elusive. Although Ocean Drilling Program (ODP) and Deep Sea Drilling Program (DSDP) legs have drilled extant oceanic plateaus in the ocean basins, the vast majority of the stratigraphic sequence of oceanic plateaus remains generally unsampled and undescribed. Oceanic plateaus are enormous vol- canic edifices (2–4 km high above the ocean floor) that are isolated from continents and form upon mid-ocean ridges, extinct arcs, detached or sub- merged continental fragments, or in intraplate set- tings [Coffin et al., 2006]. The basalts that form oceanic plateaus have a better chance of avoiding interaction with continental lithosphere than basalts erupted along the margins or in the interiors of continents [Kerr and Mahoney, 2007]. [3] An enduring issue involving the geochemistry of flood basalt provinces has been the origin of high- and low-titanium basalts within the flood basalt stratigraphy [e.g., Arndt et al., 1993]. Nu- merous LIPs have been found to possess two or more distinguishable groups of basalts based on titanium contents (e.g., Siberia [Wooden et al., 1993]; Emeishan [Xu et al., 2001]; Central Atlantic Magmatic Province [Nomade et al., 2002]; Karoo [Cox et al., 1967]; Ferrar [Hornig, 1993]; Paraná- Etendeka [Peate, 1997]; Deccan [Melluso et al., 1995]; Ethiopia [Pik et al., 1998]; Columbia River Basalts [Hooper and Hawkesworth, 1993]). In several of these provinces, the high- and low- titanium basalts are geographically distributed within the province, and in several provinces these lava types have a distinct stratigraphic distribution. However, all of these LIPs formed upon continen- tal crust and involved interaction with metasomat- ized lithospheric mantle or continental crust during parts of their eruptive histories. [4] The Wrangellia flood basalts in Alaska are remnants of an oceanic plateau that erupted in the eastern Panthalassic Ocean over <5 Ma in the Middle to Late Triassic, with accretion to western North America occurring in the Late Jurassic or Early Cretaceous [Jones et al., 1977]. The Wran- gellia flood basalts form thick successions of flood basalts bounded by marine sediments that extend over areas of Alaska, Yukon, and British Columbia (>2300 km in length). In south central Alaska, the flood basalt stratigraphy overlies late Paleozoic oceanic arc crust and marine sediments and is overlain by Late Triassic limestone. Most of the 3.5–4 km-thick sequence of flood basalts in Alaska erupted subaerially; however, in areas of Alaska there are pillowed and volcaniclastic basalts in the lower part of the volcanic stratigraphy. [5] The Wrangellia oceanic plateau in Alaska is unusual as it is part of one of the only known LIPs that was constructed on the volcanic sequences of an older island arc. This raises the possibility that the erupted basalts contain a component from the subarc lithospheric mantle of this late Paleozoic arc. This is an intriguing hypothesis to test since both high- and low-titanium basalts have been recognized in the volcanic stratigraphy in Alaska as a result of this study, and thus may provide a direct comparison to CFBs built on older continen- tal lithosphere. [6] This study examines the volcanic stratigraphy, petrography, and geochemistry of flood basalts in the Wrangell Mountains and Alaska Range in south central Alaska and assesses the nature of the source and the origin of high- and low-titanium basalts in this part of the accreted Wrangellia oceanic plateau. A mantle plume origin was pro- posed for Wrangellia flood basalts by Richards et al. [1991] based on the large volume of flood basalts erupted in a short duration, the absence of evidence of rifting, and evidence of uplift prior to eruption of the flood basalts. The only previous modern analytical study of the Wrangellia flood basalts in Alaska involved major and trace element chemistry, and Sr, Nd, and Pb isotopic analyses, of nine basalts from the Wrangell Mountains [Lassiter et al., 1995]. This present study is part of a larger research project on the origin and evolution of the Triassic Wrangellia flood basalts in Alaska, Yukon, and British Columbia [Greene et al., 2008a, 2008b]. These areas (each 400 km in length, for a total length of 2300 km) have different volcanic stratigraphy, distinct geochemical charac- teristics (and similarities), and they overlie Paleo- Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 2 of 34 zoic basement of different age and lithology. Exploring the internal stratigraphy and geochem- istry of the accreted Wrangellia oceanic plateau provides constraints on the composition of less accessible examples in the ocean basins such as the Ontong Java and Kerguelen Plateaus. 2. Geologic Setting 2.1. Wrangellia in Alaska [7] The Wrangellia Terrane, or Wrangellia, was defined by Jones et al. [1977] as a set of fault- bound crustal blocks with similar-aged flood basalts overlain by limestone along the margin of western North America (Figure 1). The Wrangellia flood basalts have been mapped as the Nikolai Formation in Alaska and Yukon where they directly overlie shale with Middle to Late Ladinian (235– 232 Ma) Daonella. Wrangellia may have joined with parts of the Alexander Terrane, primarily in southeast Alaska, as early as the Late Pennsylvanian [Gardner et al., 1988] and may have been in close proximity to the Peninsular Terrane of southern Alaska by the Late Triassic [Rioux et al., 2007]. [8] Wrangellia extends 450 km in an arcuate belt across southern Alaska in the Wrangell Mountains, Alaska Range, and Talkeetna Mountains (Figure 1). The northwest margin of Wrangellia is one of the most prominent geophysical features in south cen- tral Alaska and is exposed along the Talkeetna Suture Zone [Glen et al., 2007]. The suture be- tween Wrangellia and transitional crust to the northwest is well-defined geophysically [Glen et al., 2007] and lies directly in the axis of the major orocline of southern Alaska, where structures curve from northwest- to northeast-trending [e.g., Plafker Figure 1. Simplified map of south-central Alaska showing the distribution of the Nikolai Formation (black), derived from the GIS-based digital map compilations of Wilson et al. [1998, 2005] and J. M. Schmidt (personal communication, 2006). The three main areas that were studied are outlined with boxes and indicated in the legend. The inset shows the extent of the Wrangellia flood basalts (green) in Alaska, Yukon, and British Columbia, with a red box indicating the map location. The red lines are faults and gray lines are glaciers. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 3 of 34 et al., 1994]. Wrangellia is bounded by the Denali Fault to the northeast and extends more than 300 km to the southeast in Yukon. 2.1.1. Wrangell Mountains [9] Wrangellia stratigraphy is well-exposed in a northwest-trending belt extending 100 km along the southern flank of the Wrangell Mountains in Wrangell-St. Elias National Park (Figure 2). The Nikolai Formation unconformably overlies the Skolai Group, which comprises Pennsylvanian to Early Permian volcanic arc sequences and marine sediments of the Station Creek and Hasen Creek Formations, respectively [Smith and MacKevett, 1970; Figure 2]. The Skolai Group is intruded by mafic and ultramafic intrusive bodies related to the Nikolai basalts. Exposures of the Nikolai basalts cover 1057 km2 in Wrangell-St. Elias National Park and are approximately 3.5–4 km in total thickness. Over 3.5 km of marine sedimentary rocks, ranging in age from Late Triassic to Late Jurassic, overlie the Nikolai Formation in the Wrangell Mountains [MacKevett et al., 1997], and in turn are overlain by Cretaceous sedimentary sequences and the Miocene to Holocene Wrangell volcanics [MacKevett, 1978; Richter et al., 1990]. 2.1.2. Eastern Alaska Range [10] The Nikolai Formation in the eastern Alaska Range and small areas of the Talkeetna Mountains is exposed over 666 km2 and is 3.5–4 km thick in the Amphitheater and Clearwater Mountains (Figure 1). Volcanic and marine sedimentary sequences similar to the late Paleozoic successions in the Wrangell Mountains underlie the Nikolai basalts in the Alaska Range [Nokleberg et al., 1994]. The most significant occurrence of plutonic rocks associated with the Nikolai basalts occurs in the Amphitheater Mountains within a broad syn- form. Sequences overlying the Nikolai basalts are poorly exposed in the Amphitheater Mountains but preserve interbedded volcanic and sedimentary horizons that give way to fine-grained marine sedimentary strata. 2.2. Age of the Nikolai Formation [11] Biostratigraphy and geochronology provide bounds on the age and duration of emplacement of the Nikolai basalts. Fossil assemblages in finely Figure 2. Geologic map and stratigraphy of the Wrangell Mountains, Alaska (map location shown by box 1 in Figure 1). (a) Stratigraphic column depicts late Paleozoic to Jurassic units on the south side of the Wrangell Mountains, derived from Smith and MacKevett [1970] and MacKevett [1978]. (b) Simplified map showing the distribution of the Nikolai Formation (green) in the Wrangell Mountains, derived from the GIS-based digital map compilation of Wilson et al. [2005]. The four areas of field study are outlined with labeled boxes. The red lines are faults, gray lines are glaciers, and blue lines are rivers. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 4 of 34 laminated shale immediately beneath the Nikolai basalts in the Wrangell Mountains indicate a Mid- dle to Late Ladinian age (235–232 Ma) [Jones et al., 1977; C. A. McRoberts, personal communica- tion, 2007] and fossils in limestone disconformably overlying the Nikolai Formation are Late Carnian to Early Norian (223–212 Ma) [Armstrong and MacKevett, 1977; Plafker et al., 1989]. Five 40Ar/39Ar plateau ages for hornblende and biotite from intrusive rocks in the Amphitheater Moun- tains in the Alaska Range, which are interpreted to be comagmatic with Nikolai basalts, indicate for- mat ion of these rocks at 231 – 225 Ma [Bittenbender et al., 2007; Schmidt and Rogers, 2007]. Three Nikolai basalt samples from the Wrangell Mountains yielded 40Ar/39Ar step-heating ages of 228.3 ± 5.2, 232.8 ± 11.5, and 232.4 ± 11.9 Ma [Lassiter, 1995]. 3. Volcanic Stratigraphy [12] Field studies in Alaska focused in three gen- eral areas where parts of the entire flood basalt Figure 3. Photographs of the base of the Nikolai Formation in the Wrangell Mountains, Alaska. (a) Westward dipping Paleozoic arc volcanic rocks of the Station Creek Formation overlain by Early Permian shale and limestone (Phc-Hasen Creek Formation; Pgh-Golden Horn Limestone Lentil), isolated lenses of Middle Triassic ‘‘Daonella beds’’ (TRd), basalt flow-conglomerate with local pillows, and massive subaerial flows on the north side of Skolai Creek. Photograph by Ed MacKevett Jr. (b) Close-up photograph of area b in Figure 3a. (c) Close-up photograph of area c in Figure 3b showing basal flow-conglomerate with clasts of rounded cobbles of white limestone (<20 cm) derived from Golden Horn Limestone Lentil and red basalt (<40 cm) from Station Creek Formation. Pen (14 cm) in middle of photograph for scale. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 5 of 34 stratigraphy are well exposed: the southern flank of the Wrangell Mountains and the Amphitheater and Clearwater Mountains in the southern part of the eastern Alaska Range (Figure 1). [13] In the Wrangell Mountains, four areas were examined and sampled: Skolai Creek, Glacier Creek, Hidden Lake Creek, and Nugget Creek (Figure 2). The volcanic stratigraphy in the Wran- gell Mountains is predominantly subaerial flows with <100 m of submarine flows along the base. The base of the Nikolai Formation is exposed at Skolai Creek where basalt flow-conglomerate, pil- low breccia, and minor pillow basalt unconform- ably overlie the Paleozoic Sicker Group (Figures 2 and 3). Middle to upper portions of the flood basalt stratigraphy are well exposed above Glacier Creek, where massive maroon- and green-colored flows form monotonous sequences with amygdaloidal- rich horizons and no discernible erosional surfaces or sediments between flows (Figure 4). The top of the flood basalts are best exposed around Hidden Lake Creek where a sharp contact between Nikolai basalts and overlying Chitistone Limestone is mostly a smooth surface with minimal evidence of weathering [Armstrong and MacKevett, 1982] (Figure 5 ). [14] In the Amphitheater Mountains, fieldwork was concentrated in five areas: Glacier Gap Lake, Landmark Gap Lake, Tangle Lakes (West), Sugar- loaf Mountain, and Rainy Creek (Figure 6). The Amphitheater Mountains south of the Eureka Creek Fault form a broad synform consisting of flood basalts (3.5 km thick) with basal sill com- plexes and associated mafic and ultramafic rocks exposed along the outer margins. The lower 500 m of volcanic stratigraphy are submarine Figure 4. Photograph of 1000 m of continuous subaerial flood basalt stratigraphy at the top of the Nikolai Formation along Glacier Creek in the Wrangell Mountains, Alaska. The yellow line marks the contact between Nikolai basalts and the overlying Chitistone Limestone. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 6 of 34 flows and the stratigraphy above this is mostly massive subaerial flows (<15 m thick). The lowest part of 1000 m of sills and submarine flows (e.g., Lower Tangle Lakes) consists of nonfossiliferous shale and siliceous argillite (<4 m thick) interbed- ded with massive mafic sills (2–30 m thick), in turn overlain by pillow basalt (Figure 7). Sills interbedded with thinly bedded basaltic sandstone and minor hyaloclastite also occur higher in the submarine stratigraphy (Figures 6 and 7). [15] A small segment of Wrangellia in the northern part of the Amphitheater Mountains consists of a heterogeneous assemblage of mafic and ultramafic plutonic and volcanic rocks that forms a wedge between the Broxson Gulch Thrust and the Eureka Creek Fault (Figure 6). These units are distinct from those within the synform and therefore a suite of eight samples, including several altered olivine- bearing picritic tuffs (Rainy Creek picrites), were collected for comparison to Nikolai basalts within the synform. [16] In the Clearwater Mountains (40 km west of the Amphitheater Mountains), the lower <400 m of the volcanic stratigraphy is submarine flows and the remainder of the stratigraphy is primarily subaerial flows (see Auxiliary Material).1 The lowest flows are pillow basalt that directly overlie thin beds of shale and argillite (<3 m thick). Picritic pillow lavas have been found in the submarine stratigraphy. The upper parts of the volcanic stratigraphy contain subaerial flows (or 1Auxiliary materials are available in the HTML. doi:10.1029/ 2008GC002092. Figure 5. Photographs showing the top of the Nikolai Formation in the Wrangell Mountains, Alaska. (a) Chitistone Limestone overlying the Nikolai Formation above Hidden Creek in the Wrangell Mountains. Faulting has offset the contact. (b) Close-up photograph of uppermost Nikolai flow and base of the Chitistone Limestone from where Figure 5a was taken. (c) Cobbles <10 cm long along the contact between the Chitistone Limestone and Nikolai Formation. The oxidized cobbles are subangular, closely packed, aligned along their long axes, and are glomeroporphyritic basalt identical to the uppermost flows of the Nikolai Formation. Sledgehammer handle (4 cm wide) for scale. Thinly bedded siltstone also occurs along the contact. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 7 of 34 sills) with columnar jointing, minor occurrences of tuff and volcanic breccia, and limestone and argillite lenses interbedded with flows are overlain by fine-grained sediments with diagnostic index fossils (bivalve Halobia and ammonoid Tropites [Smith, 1981]). [17] A total of 111 samples of the Nikolai Forma- tion and several Paleozoic, late Mesozoic, and Cenozoic volcanic and sedimentary rocks were collected for petrography and geochemical analy- sis. Fifty-three of these samples were selected for geochemistry based on the visual degree of alter- ation (see Auxiliary Material) and are grouped into high- and low-titanium basalts, sills, and picrites based on geochemistry. The sample preparation and analytical methods for whole-rock chemistry, major elements, trace elements, and Sr, Nd, Hf, and Pb isotopes are described in Appendix A. 4. Whole-Rock Chemistry 4.1. Major and Trace Element Compositions [18] The most noteworthy feature of the major element chemistry of the Nikolai Formation is two clearly distinguishable groups of high- and low-titanium basalt (Figure 8). The low-titanium basalts range from 0.4 to 1.2 wt % TiO2 and the high-titanium basalts range from 1.6 to 2.4 wt % TiO2 (Figure 8; Table 1). The high-titanium basalts have a limited range in MgO (5.7–7.9 wt % MgO, except for one plagioclase-rich flow with 4.8 wt % Figure 6. Simplified geologic map and stratigraphy of the Amphitheater Mountains, Alaska (map location shown by box 2 in Figure 1). (a) Stratigraphic column with sample lithologies and estimated vesicularity for flood basalts from the lower part of the volcanic stratigraphy, derived from three traverses marked by red lines in Figure 6b. Vesicularity estimated visually from thin-sections. (b) Generalized geology of the Nikolai Formation and related plutonic rocks in the Amphitheater Mountains. Five main field areas are outlined with numbered boxes (see legend). Map derived from Nokleberg et al. [1992] and the digital compilation of Wilson et al. [1998]. (c) Schematic cross- section of Amphitheater Mountains from A to A’ in Figure 6b, adapted from Nokleberg et al. [1985]. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 8 of 34 MgO) and SiO2 (49.2–52.1 wt %), whereas the low-titanium basalts extend to higher MgO and have a significantly larger range in MgO (6.4– 12.0 wt %) and SiO2 (46.7–52.2 wt %). The low- titanium basalts have noticeably higher Mg # (mean Mg # = 60) than the high-titanium basalts (mean Mg # = 50; Mg # = molar MgO/(MgO + FeOT) 100, where FeOT refers to all Fe expressed Figure 7. Photographs of the base of the Nikolai Formation in the Amphitheater Mountains, east central Alaska Range, Alaska (from the Tangle Lakes (West) area shown in Figure 6). (a) Basal sills and sediments beneath submarine flows. Letters denote locations of other photographs. (b) Fissile shale (4 m thick) and a mafic sill from the lowermost exposure of shale. (c) Pillow basalt with shale between pillows lying directly above shale similar to Figure 7b. (d) Pillow basalt (pillow tubes are <1 m diameter in cross-section) in the lowermost flow (13 m thick) in the Tangle section. Figure 7c is from the base of this flow. Sledgehammer (80 cm long) for scale. (e) Sequence of at least four massive sills (<8 m thick) interbedded with fine-grained tuff (<2 m thick). Tuff layers interbedded with sills contain plagioclase crystals (<0.5 mm), curvilinear shards, and local areas of volcanic breccia containing basaltic clasts with abundant small acicular plagioclase (<0.5 mm). Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 9 of 34 as FeO). Nearly all of the Nikolai basalts in Alaska fall within the tholeiitic field in a total alkalis versus silica plot, with low-titanium basalts generally having lower total alkalis than the high-titanium basalts. The low-titanium basalts exhibit broadly decreasing trends of TiO2, FeOT, and Na2O with increasing MgO (Figure 8) and have higher loss-on- ignition (LOI; mean LOI = 2.7 ± 1.3 wt %) than the high-titanium basalts (mean LOI = 1.9 ± 1.5 wt %; Table 1). Low-titanium basalts with >8 wt% MgO have higher concentrations of Ni than the high- titanium basalts and the three picrite samples have noticeably higher Ni concentrations (525– 620 ppm) than all basalts. Both the high- and low-titanium basalts have a large range in CaO, which appears to be independent of MgO variation. A single Clearwater picrite (13.6 wt % MgO) and two Rainy Creek picrites (15.5–16.2 wt % MgO) have higher MgO with similar TiO2, FeOT, and alkali contents to the low-titanium basalts, however, the Rainy Creek picrites have lower Al2O3. The basal flow-conglomerate from the Wrangell Moun- tains has distinct major element chemistry compared to the other Nikolai basalts. Nikolai basalts in Alaska are lower in total alkalis than basalts from Yukon due to alkali metasomatism during alteration of the Yukon basalts [Greene et al., 2008a]. Figure 8. Whole-rock major element variation diagrams versus MgO for the Nikolai Formation in Alaska with fields for the Nikolai Formation in Yukon [Greene et al., 2008a]. The boundary of the alkalic and tholeiitic fields is that of MacDonald and Katsura [1964]. Total iron expressed as FeO and oxides are plotted on an anhydrous, normalized basis. Note the clear distinction between the high- and low-titanium basalts in Figure 8b and the difference in alkali contents between the Nikolai basalts in Alaska and Yukon in Figure 8a. Fields for Nikolai basalts in Yukon are green for low-Ti basalts and red for high-Ti basalts. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 10 of 34 Table 1 (Sample). Major Element and Trace Element Abundances in Whole-Rock Samples of Nikolai Basalts, Alaskaa [The full Table 1 is available in the HTML version of this article at http://www.g-cubed.org] Sample 5707A3 5708A2 5710A2 5710A3 5712A2 5714A1 5714A3 5715A1 (1) 5715A1 (2) 5715A5 Group HI-TI HI-TI HI-TI HI-TI HI-TI HI-TI HI-TI HI-TI HI-TI LOW-TI Area WM WM WM WM WM WM WM WM WM WM Flow FLO FLO FLO FLO FLO FLO FLO FLO FLO FLO UTM EW 6816521 6813830 6838676 6836850 6838178 6826371 6826390 6827794 6827794 6828050 UTM NS 430777 428595 356035 356266 353987 384783 384806 383399 383399 383641 Unnormalized Major Element Oxides SiO2 49.74 48.40 48.81 50.02 49.90 49.31 50.21 49.61 49.41 50.25 TiO2 1.96 2.36 2.4 1.95 1.89 1.66 1.6 1.69 1.68 1.14 Al2O3 13.37 13.49 15.21 14.45 13.76 15.58 16.01 15.56 15.75 16.69 Fe2O3* 14.05 16.14 12.94 13.39 13.76 13.21 10.99 13 12.97 10.39 MnO 0.27 0.27 0.23 0.18 0.24 0.17 0.16 0.2 0.2 0.18 MgO 6.69 5.89 6.85 6.56 6.74 6.6 6.64 6.63 6.62 7.94 CaO 10.61 10.09 9.16 8.56 11.35 10.8 9.97 11.09 11.04 9.48 Na2O 2.64 2.47 3.15 3.56 1.87 2.08 3.77 1.84 1.82 3.36 K2O 0.29 0.61 0.58 1.03 0.22 0.42 0.28 0.2 0.2 0.67 P2O5 0.16 0.23 0.21 0.18 0.16 0.15 0.14 0.15 0.14 0.09 Total 99.78 99.95 99.54 99.88 99.89 99.98 99.77 99.97 99.83 100.19 LOI 1.68 1.41 2.37 2.47 1.28 2.39 3.12 0.84 1.84 3.57 Trace Elements La 10.32 8.08 6.56 6.56 3.74 Ce 24.25 21.79 17.07 17.07 10.69 Pr 3.66 2.90 2.35 2.35 1.49 Nd 18.83 14.73 12.20 12.20 7.68 Sm 5.22 4.19 3.51 3.51 2.32 Eu 1.73 1.43 1.25 1.25 0.90 Gd 5.57 4.17 3.80 3.80 2.55 Tb 1.02 0.77 0.72 0.72 0.50 Dy 6.84 5.04 4.77 4.77 3.34 Ho 1.35 0.99 0.98 0.98 0.69 Er 4.02 2.85 2.86 2.86 1.98 Tm 0.51 0.33 0.36 0.36 0.25 Yb 3.58 2.37 2.59 2.59 1.77 Lu 0.53 0.36 0.40 0.40 0.28 Sc 44.06 42.52 41.17 41.17 38.50 V 362 411 349 337 346 329 276 354 352 249 Cr 165 62 167 119 133 156 282 165 167 460 Co 47 45 44 44 39 Ni 75 57 89 69 73 82 81 85 85 116 Cu 19 1067 126 126 64 Zn 121 176 126 108 113 109 88 110 111 68 Ga 19 20 21 19 19 19 17 20 19 15 Rb 3.4 9.7 6.1 15 2.2 5.2 2.6 1 1 8.5 Sr 237 162 263 481 184 334 394 184 184 437 Y 28.1 36.1 31.6 27.8 25.8 26.2 22.6 26 26.2 18.3 Zr 113 148 145 115 110 99 93 98 98 60 Nb 10.1 12.5 12.2 9.7 9.9 7.7 7.3 7.7 7.7 4.4 Cs 0.08 0.14 0.28 0.28 0.83 Ba 79 108 147 246 70 63 56 55 56 129 Hf 4.10 3.15 2.78 2.78 1.79 Ta 0.74 0.67 0.48 0.48 0.30 Pb 1.59 0.81 0.52 0.52 0.44 Th 0.98 0.72 0.64 0.64 0.34 a Major elements are measured in wt% oxide and trace elements are measured in ppm. Abbreviations for group are HI-TI, high-titanium; LOW- TI, low-titanium; RC, Rainy Creek; RCPIC, Rainy Creek picrite; CWPIC, Clearwater picrite. Abbreviations for flow are: FLO, massive flow; PIL, pillow basalt; FLO-BRE, flow-conglomerate-pillow breccia; SIL, sill; TUF, tuff. Abbreviations for area are: WM, Wrangell Mountains; TANGLE, Tangle Lakes; GLAC, Glacier Gap Lake; CLEAR, Clearwater Mountains; RAINY, Rainy Creek. Sample locations are given using the Universal Transverse Mercator (UTM) coordinate system (NAD83; zones 6 and 7). XRF analyses were performed at University of Massachusetts Ronald B. Gilmore XRF Laboratory. Fe2O3* is total iron expressed as Fe2O3. LOI is loss-on-ignition. Totals have not been resummed using the LOI value. Elements by XRF: Sc, V, Cr, Ni, Zn, Ga, Rb, Sr, Y, Zr, Nb, Ba. Elements by ICP-MS: REE, Co, Cu, Cs, Hf, Ta, Pb, Th, U. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 11 of 34 [19] The low-titanium basalts are characterized by a range of flat and slightly light rare earth element (LREE) -depleted chondrite-normalized REE pat- terns (mean La/SmCN = 0.8 ± 0.5, except one LREE-enriched sample) with flat, parallel heavy REE (HREE) segments (mean Dy/YbCN = 1.0 ± 0.2; Figure 9). The high-titanium basalts form a tight range of parallel LREE-enriched patterns (mean La/YbCN = 2.3 ± 0.9) with higher REE abundances (mean YbCN = 16.1 ± 6.4) than the Figure 9. Whole-rock REE and other incompatible-element concentrations for the Nikolai Formation in Alaska. (a, c, and e) Chondrite-normalized REE patterns for high-titanium basalts, low-titanium basalts, and picrites, respectively, from field areas in southern Alaska. (b, d, and f) Primitive mantle-normalized trace element patterns for high-titanium basalts, low-titanium basalts, and picrites, respectively. All normalization values are fromMcDonough and Sun [1995]. Depleted MORB average from Salters and Stracke [2004]. Note the clear distinction between LREE-enriched high- titanium basalt andmostly LREE-depleted low-titanium basalts. Trace element patterns for the basal flow-conglomerate and one Clearwater sample are not shown in Figure 9d for clarity. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 12 of 34 low-titanium basalts (mean YbCN = 11.0 ± 2.2; Figure 9). Several low-titanium basalts from the Amphitheater Mountains have positive Eu anoma- lies (Figure 9). Two high-titanium basalts from the Wrangell Mountains have patterns with flatter HREE segments. The basal flow-conglomerate from the Wrangell Mountains has a distinct LREE-enriched pattern (La/SmCN = 2.7) with a flat HREE segment (Dy/YbCN = 1.2). The Rainy Creek picrites are LREE-enriched (La/YbCN = 2.8–3.1) and the REE pattern of the Clearwater picrite is LREE-enriched (La/SmCN = 1.9) with a flat HREE segment (Dy/YbCN = 1.0). [20] The low-titanium basalts have mostly parallel, primitive mantle-normalized trace element patterns with pronounced high field strength element (HFSE) depletions, especially for Nb, Ta, and Zr, relative to LILE and REE (Figure 9), and the HFSE (Nb and Zr) form linear trends in binary diagrams (Figure 10). The LILE segments of trace element patterns for low-titanium basalts are parallel and each of the patterns has a pronounced positive Sr anomaly, relative to Nd and Sm. The high-titanium basalts form a tight range of parallel, concave- downward extended trace element patterns with negative Pb anomalies, relative to Ce and Pr, and small negative K anomalies, relative to U and Nb Figure 10. Whole-rock trace element concentration (in ppm) variations and ratios for the Nikolai Formation in Alaska (except Figure 10b is versus MgO in wt. %), with fields for the Nikolai Formation in Yukon. (a) Nb versus Zr. (b) Nb/La versus MgO. (c) Th versus Hf. (d) Sr versus Y/Nb (Yukon fields not shown). Note the clear distinction between the high- and low-titanium basalts in each of the plots. Fields for Nikolai basalts in Yukon are green for low- Ti basalts and red for high-Ti basalts. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 13 of 34 (Figure 9). The LILE in the high-titanium basalts are slightly depleted relative to the HFSE and LREE. The Clearwater picrite is depleted in HFSE with a positive Sr anomaly, similar to the low- titanium basalts, whereas the Rainy Creek picrites have gently negative-sloping patterns with negative Sr anomalies (Figure 9). 4.2. Sr-Nd-Hf-Pb Isotopic Compositions [21] The high- and low-titanium Wrangellia basalts in Alaska have distinct Hf and Sr isotope ratios (Figure 11). The low-titanium basalts have higher initial eHf (+13.7 to +18.4) and 87Sr/86Sr (0.70422– 0.70554) than the high-titanium basalts (initial eHf = +9.7 to +10.7, initial 87Sr/86Sr = 0.70302– 0.70376), except for sample 5715A5, which has anomalous chemistry (age correction to 230 Ma; Figure 11; Tables 2 and 3). The low-titanium basalts have a narrower range in initial eNd (+4.6 to +5.4) than the high-titanium basalts (initial eNd = +6.0 to +8.1) and a wider range in initial eHf, except for three low-titanium samples with higher initial eNd (+7.0 to +7.6). The basal flow-conglomerate from the Wrangell Mountains has similar initial Sr, Nd, and Hf isotopic compositions to the high-titanium basalts. The Clearwater picrite lies between the high- and low-titanium basalts in initial eHf and has the lowest initial eNd and initial 87Sr/86Sr at the upper end of the range of all samples. The two Rainy Creek picrites have similar Sr, Nd, and Hf Figure 11. Whole-rock Sr, Nd, and Hf isotopic compositions for the Nikolai Formation in Alaska. (a) 176Hf/177Hf versus 176Lu/177Hf. (b) 143Nd/144Nd versus 147Sm/144Nd. (c) Initial eNd versus 87Sr/86Sr; age correction to 230 Ma. (d) Initial eHf versus eNd. (e) Initial eHf versus 87Sr/86Sr. Average 2s error bars are shown in a corner of Figures 11a–11e. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 14 of 34 T a b le 2 . S r an d N d Is o to p ic G eo ch em is tr y o f W h o le -R o ck S am p le s o f N ik o la i B as al ts , A la sk a S am p le G ro u p a A re ab R b (p p m ) S r (p p m ) 8 7 S r/ 8 6 S r 2 s m 8 7 R b /8 6 S r 8 7 S r/ 8 6 S r t 2 3 0 M a S m (p p m ) N d (p p m ) 1 4 3 N d /1 4 4 N d 2 s m e N d 1 4 7 S m /1 4 4 N d 1 4 3 N d /1 4 4 N d t 2 3 0 M a e N d (t ) 5 7 0 8 A 2 H i- T i W M 9 .7 1 6 2 0 .7 0 3 7 7 6 7 0 .1 7 3 3 0 .7 0 3 2 1 5 .2 2 1 8 .8 3 0 .5 1 3 0 1 1 5 7 .3 0 .1 6 7 7 0 .5 1 2 7 6 8 .1 5 8 0 1 A 2 H i- T i C L 1 .7 2 2 5 0 .7 0 3 3 6 5 8 0 .0 2 1 9 0 .7 0 3 2 9 5 .5 5 2 1 .1 0 0 .5 1 2 9 3 4 7 5 .8 0 .1 5 9 2 0 .5 1 2 6 9 6 .9 5 7 1 9 A 5 H i- T i W M 5 .9 2 0 0 0 .7 0 3 3 4 4 8 0 .0 8 5 4 0 .7 0 3 0 6 4 .4 5 1 6 .2 6 0 .5 1 2 9 8 8 6 6 .8 0 .1 6 5 3 0 .5 1 2 7 4 7 .7 5 8 0 1 A 5 H i- T i C L 5 .9 1 8 7 0 .7 0 3 3 8 9 8 0 .0 9 1 3 0 .7 0 3 0 9 4 .2 5 1 5 .5 1 0 .5 1 2 9 3 7 6 5 .8 0 .1 6 5 9 0 .5 1 2 6 9 6 .7 5 7 1 2 A 2 H i- T i W M 2 .2 1 8 4 0 .7 0 3 1 7 9 8 0 .0 3 4 6 0 .7 0 3 0 7 4 .1 9 1 4 .7 3 0 .5 1 2 9 9 7 6 7 .0 0 .1 7 2 0 0 .5 1 2 7 4 7 .7 5 7 2 6 A 1 H i- T i T A 2 .1 2 3 9 0 .7 0 3 8 4 4 7 0 .0 2 5 4 0 .7 0 3 7 6 4 .0 7 1 4 .3 5 0 .5 1 2 9 0 8 7 5 .3 0 .1 7 1 3 0 .5 1 2 6 5 6 .0 5 8 1 0 A 1 0 H i- T i T A 2 .6 2 3 1 0 .7 0 3 4 4 8 9 0 .0 3 2 6 0 .7 0 3 3 4 3 .9 5 1 3 .9 8 0 .5 1 2 9 1 8 6 5 .5 0 .1 7 0 7 0 .5 1 2 6 6 6 .2 5 7 1 5 A 1 H i- T i W M 1 .0 1 8 4 0 .7 0 3 6 1 9 7 0 .0 1 5 7 0 .7 0 3 5 7 3 .5 1 1 2 .2 0 0 .5 1 3 0 1 7 7 7 .4 0 .1 7 3 8 0 .5 1 2 7 6 8 .1 5 7 1 5 A 5 L o w -T i W M 8 .5 4 3 7 0 .7 0 3 6 0 2 8 0 .0 5 6 3 0 .7 0 3 4 2 2 .3 2 7 .6 8 0 .5 1 3 0 3 0 5 7 .6 0 .1 8 2 9 0 .5 1 2 7 5 8 .1 5 8 0 2 A 5 L o w -T i C L 3 .0 2 5 2 0 .7 0 4 9 4 2 6 0 .0 3 4 5 0 .7 0 4 8 3 2 .1 9 6 .6 8 0 .5 1 3 0 0 0 6 7 .1 0 .1 9 8 0 0 .5 1 2 7 0 7 .0 5 8 1 0 A 6 L o w -T i T A 2 .0 1 7 0 0 .7 0 4 7 0 4 7 0 .0 3 4 0 0 .7 0 4 5 9 1 .5 5 4 .5 2 0 .5 1 2 9 2 4 6 5 .6 0 .2 0 7 0 0 .5 1 2 6 1 5 .3 5 8 1 0 A 1 L o w -T i T A 0 .9 1 5 1 0 .7 0 4 7 2 1 7 0 .0 1 7 2 0 .7 0 4 6 6 1 .2 6 3 .3 1 0 .5 1 2 9 6 3 5 6 .3 0 .2 3 0 3 0 .5 1 2 6 2 5 .4 5 7 2 7 A 7 L o w -T i T A 1 .5 1 5 5 0 .7 0 4 8 6 5 9 0 .0 2 8 0 0 .7 0 4 7 7 1 .3 0 3 .8 6 0 .5 1 2 9 0 6 7 5 .2 0 .2 0 3 8 0 .5 1 2 6 0 5 .0 5 8 0 2 A 2 L o w -T i C L 2 .1 3 0 3 0 .7 0 5 6 0 4 8 0 .0 2 0 1 0 .7 0 5 5 4 1 .3 1 4 .0 4 0 .5 1 2 8 7 2 7 4 .6 0 .1 9 5 9 0 .5 1 2 5 8 4 .6 5 7 1 9 A 1 B as al W M 2 5 .4 1 5 8 0 .7 0 5 1 3 8 7 0 .4 6 5 2 0 .7 0 3 6 2 4 .2 6 2 0 .6 5 0 .5 1 2 8 9 2 6 5 .0 0 .1 2 4 8 0 .5 1 2 7 0 7 .1 5 7 2 5 A 4 S il l (H i- T i) T A 1 6 .5 2 0 7 0 .7 0 3 7 7 5 8 0 .2 3 0 6 0 .7 0 3 0 2 4 .3 0 1 5 .1 6 0 .5 1 2 9 1 6 7 5 .4 0 .1 7 1 5 0 .5 1 2 6 6 6 .2 5 7 2 7 A 2 S il l (L o w -T i) T A 1 .7 7 6 0 .7 0 4 5 3 2 8 0 .0 6 4 7 0 .7 0 4 3 2 1 .2 2 2 .9 2 0 .5 1 3 0 9 8 6 9 .0 0 .2 5 3 1 0 .5 1 2 7 2 7 .3 5 7 2 7 A 3 S il l (L o w -T i) T A 1 .8 1 1 7 0 .7 0 4 8 7 2 8 0 .0 4 4 5 0 .7 0 4 7 3 1 .2 3 2 .9 2 0 .5 1 3 1 1 5 8 9 .3 0 .2 5 5 3 0 .5 1 2 7 3 7 .6 5 7 2 7 A 6 S il l (L o w -T i) T A 0 .6 1 2 3 0 .7 0 4 8 5 7 1 0 0 .0 1 4 1 0 .7 0 4 8 1 1 .1 1 3 .0 5 0 .5 1 2 9 3 0 7 5 .7 0 .2 2 0 3 0 .5 1 2 6 0 5 .0 5 7 2 7 A 6 (d u p ) S il l (L o w -T i) T A 0 .6 1 2 3 0 .7 0 4 8 5 1 8 0 .0 1 4 1 0 .7 0 4 8 0 1 .1 3 3 .0 9 0 .5 1 2 9 2 8 1 0 5 .7 0 .2 2 0 2 0 .5 1 2 6 0 5 .0 5 8 1 0 A 2 S il l (L o w -T i) T A 0 .8 1 4 1 0 .7 0 4 8 4 6 7 0 .0 1 6 4 0 .7 0 4 7 9 1 .1 6 3 .2 1 0 .5 1 2 9 1 7 6 5 .4 0 .2 1 8 7 0 .5 1 2 5 9 4 .8 5 8 1 0 A 4 S il l (L o w -T i) T A 0 .4 1 9 8 0 .7 0 4 2 3 5 8 0 .0 0 5 8 0 .7 0 4 2 2 1 .9 6 6 .1 2 0 .5 1 2 8 8 6 6 4 .8 0 .1 9 3 7 0 .5 1 2 5 9 4 .9 5 8 0 2 A 4 P ic ri te C L 0 .4 1 8 3 0 .7 0 5 5 3 0 9 0 .0 0 6 3 0 .7 0 5 5 1 1 .6 9 6 .6 1 0 .5 1 2 7 4 6 6 2 .1 0 .1 5 4 4 0 .5 1 2 5 1 3 .3 5 8 0 8 A 2 P ic ri te R C 6 .1 1 2 7 0 .7 0 4 1 2 4 1 0 0 .1 3 9 5 0 .7 0 3 6 7 2 .6 9 9 .8 5 0 .5 1 2 8 8 0 6 4 .7 0 .1 6 4 9 0 .5 1 2 6 3 5 .7 5 8 0 8 A 3 P ic ri te R C 2 6 .4 9 3 0 .7 0 6 3 0 7 9 0 .8 2 6 5 0 .7 0 3 6 0 3 .0 1 1 1 .5 7 0 .5 1 2 8 1 1 6 3 .4 0 .1 5 7 6 0 .5 1 2 5 7 4 .5 a H i- T i, h ig h -t it an iu m b as al t; L o w -T i, lo w -t it an iu m b as al t; B as al , b as al fl o w -c o n g lo m er at e. b A b b re v ia ti o n s fo r ar ea ar e W M , W ra n g el l M o u n ta in s; T A , T an g le L ak e; G G , G la ci er G ap L ak e; C L , C le ar w at er M o u n ta in s; R C , R ai n y C re ek . (d u p ) in d ic at es co m p le te ch em is tr y d u p li ca te . A ll tr ac e- el em en t an d is o to p ic an al y se s w er e ca rr ie d o u t at th e P C IG R . T h e an al y ti ca l m et h o d s ar e d es cr ib ed in A p p en d ix A . Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 15 of 34 isotope ratios to high-titanium basalts with slightly lower initial eNd (Figure 11). [22] The high- and low-titanium basalts have indis- tinguishable age-corrected Pb isotopic composi- tions, although the high-titanium basalts show a narrower range (Figure 12). The range of initial Pb isotopic compositions for low-titanium basalts is 206Pb/204Pb = 18.421–19.418, 207Pb/204Pb = 15.568–15.609, and 208Pb/204Pb = 37.962– 38.481 and the high-titanium basalts have 206Pb/204Pb = 18.504–18.888, 207Pb/204Pb = 15.556–15.587, and 208Pb/204Pb = 38.008–38.451 (Figure 12; Table 4). The basal flow-conglomerate has a slightly lower initial Pb isotopic composition than the high- and low-titanium basalts. The Clear- water picrite has a lower initial Pb isotope ratio than the basalts and the Rainy Creek picrites have noticeably higher initial Pb isotope ratios than the basalts (Figure 12). 5. Alteration [23] The Nikolai basalts generally preserve primary mineralogical, textural, and volcanological features and have retained most of their primary magmatic composition. Secondary minerals have replaced variable, but generally small, proportions of pri- mary minerals in the Nikolai Formation and the basalts contain zeolite to prehnite-pumpellyite facies alteration minerals (prehnite + pumpellyite + epidote + chlorite + quartz ± laumonite), primar- ily making up the amygdules [Stout, 1976; Smith, 1981;MacKevett et al., 1997]. Many of the Nikolai basalts in the synform in the Amphitheater Moun- tains are exceptionally unaltered compared to flows in the Wrangell and Clearwater Mountains. Vesicles and interpillow voids in the Amphitheater Mountains commonly remain unfilled and second- ary minerals are less common. [24] Seventeen of the 21 low-titanium basalts have LOI greater than 2.5 wt % and greater than 8 wt % MgO, whereas only four high-titanium basalts have greater than 2.5 wt % LOI and all have less than 8 wt % MgO (Figure 13). Three of the four high- titanium basalts that lie within the alkalic field are plagioclase-rich, highly amygdaloidal, and were collected near a mineralized area at the top of the Nikolai Formation. Tight linear arrays are apparent on plots of HFSE and REE (not shown) indicating negligible affect of element mobility. Only a lim- ited group of samples (5808A3, 5802A4, 5802A2, Table 3. Hf Isotopic Compositions of Whole-Rock Samples of Nikolai Basalts, Alaska Sample Groupa Areab Lu (ppm) Hf (ppm) 176Hf/177Hf 2sm eHf 176Lu/177Hf 176Hf/177Hft 230 Ma eHf(t) 5708A2 Hi-Ti WM 0.53 4.10 0.283016 5 8.6 0.0184 0.282935 11.0 5801A2 Hi-Ti CL 0.38 4.03 0.282986 6 7.6 0.0134 0.282926 10.7 5719A5 Hi-Ti WM 0.36 3.23 0.283009 6 8.4 0.0159 0.282939 11.1 5801A5 Hi-Ti CL 0.36 3.17 0.283018 7 8.7 0.0161 0.282947 11.4 5712A2 Hi-Ti WM 0.36 3.15 0.283003 6 8.2 0.0162 0.282931 10.8 5726A1 Hi-Ti TA 0.27 2.66 0.282999 6 8.0 0.0146 0.282934 11.0 5810A10 Hi-Ti TA 0.32 2.84 0.282988 6 7.6 0.0160 0.282917 10.3 5715A1 Hi-Ti WM 0.40 2.78 0.283012 5 8.5 0.0202 0.282922 10.5 5715A5 Low-Ti WM 0.28 1.79 0.283042 6 9.6 0.0223 0.282943 11.3 5802A5 Low-Ti CL 0.33 1.51 0.283299 14 18.6 0.0309 0.283162 19.0 5810A6 Low-Ti TA 0.33 0.88 0.283302 6 18.7 0.0537 0.283063 15.5 5810A1 Low-Ti TA 0.27 0.66 0.283396 5 22.1 0.0581 0.283137 18.1 5727A7 Low-Ti TA 0.33 0.70 0.283390 7 21.9 0.0670 0.283092 16.6 5802A2 Low-Ti CL 0.39 0.78 0.283358 7 20.7 0.0717 0.283039 14.7 5719A1 Basal WM 0.31 2.30 0.283008 6 8.3 0.0188 0.282924 10.6 5725A4 Sill (Hi-Ti) TA 0.30 3.08 0.282991 5 7.7 0.0141 0.282928 10.7 5727A2 Sill (Low-Ti) TA 0.27 0.80 0.283328 7 19.7 0.0489 0.283110 17.2 5727A3 Sill (Low-Ti) TA 0.26 0.87 0.283331 9 19.8 0.0425 0.283142 18.3 5727A6 Sill (Low-Ti) TA 0.24 0.57 0.283354 8 20.6 0.0602 0.283086 16.3 5810A2 Sill (Low-Ti) TA 0.27 0.66 0.283374 6 21.3 0.0581 0.283115 17.4 5810A4 Sill (Low-Ti) TA 0.32 0.96 0.283245 8 16.7 0.0481 0.283031 14.4 5802A4 Picrite CL 0.27 1.05 0.283145 6 13.2 0.0365 0.282983 12.7 5808A2 Picrite RC 0.22 1.71 0.283017 7 8.7 0.0184 0.282935 11.0 5808A3 Picrite RC 0.25 1.88 0.282977 6 7.2 0.0189 0.282893 9.5 a Hi-Ti, high-titanium basalt; Low-Ti, low-titanium basalt; Basal, basal flow-conglomerate. b Abbreviations for area are WM, Wrangell Mountains; TA, Tangle Lake; GG, Glacier Gap Lake; CL, Clearwater Mountains; RC, Rainy Creek. All trace-element and isotopic analyses were carried out at the PCIGR. The analytical methods are described in Appendix A. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 16 of 34 5725A4, 5726A1) have LILE concentrations outside the narrow range of most high- and low-titanium basalts (Figure 9) and there is no correlation be- tween LOI and LILE. All of the low-titanium basalts have positive Sr anomalies that are com- plemented with small positive Eu anomalies in most samples, and none of the high-titanium basalts have Sr anomalies (Figure 9), which indicates Sr concentrations probably represent primary values. U and Th show a linear relationship, whereas Pb and Th do not show a clear relationship (not shown), indicating some secondary mobility of Pb, especially in the low-titanium basalts. [25] Initial Hf isotopic ratios, and to a lesser extent Sr and Pb isotopic compositions, are close to magmatic compositions. Several of the more altered samples were not selected for isotopic analyses and leaching effectively removed most of the second- ary alteration products [e.g., Weis et al., 2006; Nobre Silva et al., 2008]. Whole-rock Sm/Nd ratios and age-corrected Nd isotopes, however, may be affected by the leaching procedure in submarine rocks older than 50 Ma [Thompson et al., 2008] and this may have caused a small degree of variation between Nd isotope ratios, especially for the low- titanium basalts (Figure 11). The Clearwater picrite (5802A4) was significantly affected by Pb loss and has less radiogenic age-corrected Pb isotopic ratios than the basalts (Figures 9 and 12). The correlation of LOI and 87Sr/86Sr, 206Pb/204Pb, and 238U/204Pb in the low- and high-titanium basalts Figure 12. Pb isotopic compositions of leached whole-rock samples by MC-ICP-MS for the Nikolai Formation in Alaska. Error bars are smaller than symbol size. (a) Measured 207Pb/204Pb versus 206Pb/204Pb. (b) Initial 207Pb/204Pb versus 206Pb/204Pb; age correction to 230 Ma. (c) Measured 208Pb/204Pb versus 206Pb/204Pb. (d) Initial 208Pb/204Pb versus 206Pb/204Pb. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 17 of 34 T a b le 4 . P b Is o to p ic C o m p o si ti o n s o f W h o le -R o ck S am p le s o f N ik o la i B as al ts , A la sk a S am p le G ro u p a A re ab U (p p m ) T h (p p m ) P b (p p m ) 2 0 6 P b / 2 0 4 P b 2 s m 2 0 7 P b / 2 0 4 P b 2 s m 2 0 8 P b / 2 0 4 P b 2 s m 2 3 8 U / 2 0 4 P b 2 3 5 U / 2 0 4 P b 2 3 2 T h / 2 0 4 P b 2 0 6 P b /2 0 4 P b t 2 3 0 M a 2 0 7 P b /2 0 4 P b t 2 3 0 M a 2 0 8 P b /2 0 4 P b t 2 3 0 M a 5 7 0 8 A 2 H i- T i W M 0 .3 1 0 .9 8 1 .5 9 1 9 .2 5 5 7 0 .0 0 0 6 1 5 .6 0 4 0 0 .0 0 0 5 3 8 .7 6 1 3 0 .0 0 1 4 1 2 .3 9 0 .0 9 4 0 .9 5 1 8 .8 0 6 1 5 .5 8 1 3 8 .2 8 9 5 8 0 1 A 2 H i- T i C L 0 .3 6 1 .2 4 1 .0 1 1 9 .4 4 0 4 0 .0 0 0 8 1 5 .6 1 0 0 0 .0 0 0 7 3 9 .0 2 1 7 0 .0 0 1 9 2 3 .1 1 0 .1 7 8 2 .1 7 1 8 .6 0 1 1 5 .5 6 7 3 8 .0 7 4 5 7 1 9 A 5 H i- T i W M 0 .2 5 0 .8 7 0 .8 5 1 9 .3 1 9 8 0 .0 0 0 7 1 5 .6 0 2 3 0 .0 0 0 6 3 8 .9 1 8 3 0 .0 0 1 3 1 8 .6 4 0 .1 4 6 7 .8 6 1 8 .6 4 3 1 5 .5 6 8 3 8 .1 3 6 5 8 0 1 A 5 H i- T i C L 0 .2 4 0 .8 4 0 .7 2 1 9 .6 0 2 0 0 .0 0 0 8 1 5 .6 1 9 7 0 .0 0 0 7 3 9 .1 9 5 5 0 .0 0 1 9 2 1 .5 8 0 .1 6 7 8 .2 9 1 8 .8 1 8 1 5 .5 8 0 3 8 .2 9 3 5 7 1 2 A 2 H i- T i W M 0 .2 0 0 .7 2 0 .8 1 1 9 .3 8 3 4 0 .0 0 1 1 1 5 .5 9 7 4 0 .0 0 0 9 3 9 .0 0 9 3 0 .0 0 2 4 1 6 .0 0 0 .1 2 5 9 .6 1 1 8 .8 0 2 1 5 .5 6 8 3 8 .3 2 2 5 7 2 6 A 1 H i- T i T A 0 .2 3 0 .8 6 0 .9 5 1 9 .4 5 9 4 0 .0 0 0 8 1 5 .6 1 5 8 0 .0 0 0 7 3 9 .1 5 0 6 0 .0 0 1 8 1 5 .7 3 0 .1 1 6 0 .6 8 1 8 .8 8 8 1 5 .5 8 7 3 8 .4 5 1 5 8 1 0 A 1 0 H i- T i T A 0 .2 4 0 .7 8 0 .7 6 1 9 .4 5 5 1 0 .0 0 0 7 1 5 .6 1 4 1 0 .0 0 0 5 3 9 .0 5 7 7 0 .0 0 1 4 2 0 .2 0 0 .1 5 6 8 .7 4 1 8 .7 2 1 1 5 .5 7 7 3 8 .2 6 5 5 7 1 5 A 1 H i- T i W M 0 .1 9 0 .6 4 0 .5 2 1 9 .3 8 1 5 0 .0 0 0 9 1 5 .6 0 0 2 0 .0 0 0 8 3 8 .9 5 5 7 0 .0 0 2 1 2 4 .1 5 0 .1 8 8 2 .2 2 1 8 .5 0 4 1 5 .5 5 6 3 8 .0 0 8 5 7 1 5 A 5 L o w -T i W M 0 .0 9 0 .3 4 0 .4 4 1 9 .2 5 2 0 0 .0 0 0 8 1 5 .5 9 0 8 0 .0 0 0 7 3 8 .8 0 9 6 0 .0 0 2 7 1 3 .8 8 0 .1 0 5 1 .3 3 1 8 .7 4 8 1 5 .5 6 5 3 8 .2 1 8 5 8 0 2 A 5 L o w -T i C L 0 .1 1 0 .3 4 0 .5 0 1 9 .1 7 0 8 0 .0 0 1 2 1 5 .6 0 1 9 0 .0 0 1 1 3 8 .6 8 6 1 0 .0 0 2 4 1 4 .8 0 0 .1 1 4 5 .7 9 1 8 .6 3 3 1 5 .5 7 5 3 8 .1 5 8 5 8 1 0 A 6 L o w -T i T A 0 .1 2 0 .2 8 0 .6 3 1 9 .0 1 7 8 0 .0 0 0 7 1 5 .5 9 8 0 0 .0 0 0 6 3 8 .5 4 2 8 0 .0 0 1 7 1 1 .8 4 0 .0 9 2 9 .8 7 1 8 .5 8 8 1 5 .5 7 6 3 8 .1 9 8 5 8 1 0 A 1 L o w -T i T A 0 .0 4 0 .0 9 0 .2 3 1 9 .0 0 2 5 0 .0 0 0 8 1 5 .5 9 2 7 0 .0 0 0 7 3 8 .4 6 9 7 0 .0 0 1 8 1 1 .6 4 0 .0 8 2 4 .4 8 1 8 .5 8 0 1 5 .5 7 1 3 8 .1 8 8 5 7 2 7 A 7 L o w -T i T A 0 .1 0 0 .2 9 1 .2 1 1 9 .1 1 9 0 0 .0 0 0 7 1 5 .6 0 9 9 0 .0 0 0 5 3 8 .6 6 6 7 0 .0 0 1 4 5 .5 4 0 .0 4 1 6 .0 7 1 8 .9 1 8 1 5 .6 0 0 3 8 .4 8 1 5 8 0 2 A 2 L o w -T i C L 0 .2 0 0 .5 6 0 .2 1 2 1 .6 9 0 9 0 .0 0 0 9 1 5 .7 2 4 8 0 .0 0 0 9 4 0 .5 11 9 0 .0 0 2 5 6 2 .5 7 0 .4 5 1 8 5 .2 1 1 9 .4 1 8 1 5 .6 0 9 3 8 .3 7 6 5 7 1 9 A 1 B as al W M 1 .9 1 4 .1 8 2 .9 6 1 9 .8 8 5 5 0 .0 0 0 7 1 5 .6 1 6 0 0 .0 0 0 6 3 8 .7 7 6 7 0 .0 0 2 0 4 1 .9 1 0 .3 0 9 4 .9 3 1 8 .3 6 3 1 5 .5 3 9 3 7 .6 8 2 5 7 2 5 A 4 S il l (H i- T i) T A 0 .2 5 0 .8 3 0 .6 6 1 9 .6 0 9 2 0 .0 0 1 0 1 5 .6 2 5 8 0 .0 0 0 9 3 9 .2 0 9 3 0 .0 0 1 8 2 4 .3 3 0 .1 8 8 4 .2 2 1 8 .7 2 5 1 5 .5 8 1 3 8 .2 3 8 5 7 2 7 A 2 S il l (L o w -T i) T A 0 .0 7 0 .1 7 0 .5 5 1 8 .8 6 2 5 0 .0 0 0 8 1 5 .6 0 2 1 0 .0 0 0 7 3 8 .4 7 11 0 .0 0 1 9 8 .0 5 0 .0 6 2 0 .1 1 1 8 .5 7 0 1 5 .5 8 7 3 8 .2 3 9 5 7 2 7 A 3 S il l (L o w -T i) T A 0 .0 7 0 .1 7 0 .5 0 1 8 .9 0 0 4 0 .0 0 0 9 1 5 .5 9 9 8 0 .0 0 0 8 3 8 .4 6 4 1 0 .0 0 2 4 8 .6 8 0 .0 6 2 2 .0 4 1 8 .5 8 5 1 5 .5 8 4 3 8 .2 1 0 5 7 2 7 A 6 S il l (L o w -T i) T A 0 .0 3 0 .0 7 0 .2 0 1 8 .9 0 7 6 0 .0 0 0 7 1 5 .5 9 6 7 0 .0 0 0 6 3 8 .4 9 6 0 0 .0 0 1 7 8 .3 7 0 .0 6 2 2 .3 6 1 8 .6 0 3 1 5 .5 8 1 3 8 .2 3 8 5 7 2 7 A 6 (d u p ) S il l (L o w -T i) T A 0 .0 3 0 .0 7 0 .1 8 1 8 .9 0 1 5 0 .0 0 0 5 1 5 .5 9 7 8 0 .0 0 0 5 3 8 .4 8 8 3 0 .0 0 1 4 9 .4 0 0 .0 7 2 5 .9 9 1 8 .5 6 0 1 5 .5 8 1 3 8 .1 8 9 5 8 1 0 A 2 S il l (L o w -T i) T A 0 .1 0 0 .2 7 0 .4 4 1 9 .1 9 6 8 0 .0 0 0 8 1 5 .6 0 8 9 0 .0 0 0 7 3 8 .7 7 7 6 0 .0 0 1 6 1 4 .2 1 0 .1 0 4 0 .9 7 1 8 .6 8 1 1 5 .5 8 3 3 8 .3 0 5 5 8 1 0 A 4 S il l (L o w -T i) T A 0 .0 9 0 .3 0 0 .2 6 1 9 .2 6 3 8 0 .0 0 0 8 1 5 .6 1 0 3 0 .0 0 0 7 3 8 .8 5 0 1 0 .0 0 1 8 2 3 .2 0 0 .1 7 7 7 .0 4 1 8 .4 2 1 1 5 .5 6 8 3 7 .9 6 2 5 8 0 2 A 4 P ic ri te C L 0 .3 2 0 .8 9 0 .1 3 2 3 .7 3 5 2 0 .0 0 1 8 1 5 .8 2 5 5 0 .0 0 1 3 4 2 .3 7 1 6 0 .0 0 4 3 1 6 8 .7 3 1 .2 2 4 9 1 .9 5 1 7 .6 0 6 1 5 .5 1 4 3 6 .6 9 9 5 8 0 8 A 2 P ic ri te R C 0 .2 6 0 .7 0 0 .7 6 2 1 .2 0 9 5 0 .0 0 1 4 1 5 .7 0 8 3 0 .0 0 1 2 4 0 .5 5 4 0 0 .0 0 3 0 2 3 .5 9 0 .1 7 6 4 .9 6 2 0 .3 5 3 1 5 .6 6 5 3 9 .8 0 5 5 8 0 8 A 3 P ic ri te R C 0 .3 8 1 .0 6 0 .6 5 2 1 .7 0 0 2 0 .0 0 0 9 1 5 .7 3 7 9 0 .0 0 0 8 4 0 .5 4 6 8 0 .0 0 2 4 3 9 .3 2 0 .2 9 1 1 4 .8 0 2 0 .2 7 2 1 5 .6 6 5 3 9 .2 2 3 a H i- T i, h ig h -t it an iu m b as al t; L o w -T i, lo w -t it an iu m b as al t; B as al , b as al fl o w -c o n g lo m er at e. b A b b re v ia ti o n s fo r ar ea ar e W M , W ra n g el l M o u n ta in s; T A , T an g le L ak e; G G , G la ci er G ap L ak e; C L , C le ar w at er M o u n ta in s; R C , R ai n y C re ek . (d u p ) in d ic at es co m p le te ch em is tr y d u p li ca te . A ll tr ac e- el em en t an d is o to p ic an al y se s w er e ca rr ie d o u t at th e P C IG R . T h e an al y ti ca l m et h o d s ar e d es cr ib ed in A p p en d ix A . Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 18 of 34 is a primary feature that is not apparent with age correction (Figure 13). The rather small range of initial Pb and distinct initial Hf and Sr isotopic compositions for high- and low-titanium basalts reflects the isotopic compositions of the sources of Wrangellia flood basalts in Alaska. 6. Flood Basalt Chemostratigraphy [26] Samples of the Nikolai Formation were col- lected traversing both upsection and downsection through the volcanic stratigraphy. An estimate of the relative stratigraphic position of each sample was assigned, which was then used to determine the relationship between stratigraphic position and chemical composition. Figure 14 shows sample numbers, lithologies, relative stratigraphic height, and TiO2 and MgO contents for Nikolai basalts from the three main areas of Alaska where field- work was undertaken (Figure 1). Each stratigraphic column is a combination of multiple traverses (separated by dashed lines in Figure 14). We are Figure 13. Loss-on-ignition versus MgO and isotopic ratios for the Nikolai Formation in Alaska. (a) LOI versus MgO. (b) LOI versus measured 87Sr/86Sr. (c) LOI versus measured 206Pb/204Pb. (d) LOI versus measured 238U/206Pb. The two insets show the expanded x axis for 206Pb/204Pb and 238U/206Pb. Note the generally higher LOI and MgO for the low-titanium basalts. The differences in measured 87Sr/86Sr and 206Pb/204Pb within the suites of high- and low- titanium basalts are mostly not apparent after age correction. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 19 of 34 F ig u re 1 4 Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 20 of 34 confident in the relative position of each section of stratigraphy based on the continuous exposure and minimal disruption by faults in these areas. As the trace element and isotopic variations of the basalts generally correspond with variation in TiO2 (Fig- ures 8–11), only TiO2 and MgO are shown in Figure 14. [27] In the Clearwater and Amphitheater Moun- tains, there is a clear relationship between strati- graphic position and chemical composition of the flood basalts (Figure 14). The low-titanium basalts form the lowermost several hundred meters of flows (10–15% of stratigraphy) and the high- titanium basalts form the majority of the flows (85–90% of stratigraphy) above the lowest sev- eral hundred meters. More of the low-titanium basalts and sills were sampled, partly because the lower sections of volcanic stratigraphy were more easily accessible and partly because there are more interesting relationships with pre-Nikolai sedi- ments and mafic sills and submarine units pre- served lower in the stratigraphy. The transition from low- to high-titanium basalts does not appear to coincide with the transition from submarine to subaerial flows, but almost all of the low-titanium basalts that were sampled are submarine flows. [28] In the Wrangell Mountains, there do not appear to be any low-titanium basalts, except for two anomalous samples (Figure 14). A single sample of the basal flow-conglomerate has a low titanium content (0.67 wt %), similar initial eHf to the high-titanium basalts, and anomalous La/YbCN (6.4), Ba (1277 ppm), and Th (4.18 ppm; Figures 8 and 9; Tables 1 and 3). Field observations and several other geochemical characteristics indicate the chemistry of this basal flow conglomerate is the result of considerable assimilation (30 vol %) of material derived from underlying Paleozoic sequences. The next sample upsection, 20 m above the uppermost exposure of basal flow- conglomerate in the Wrangell Mountains, does not have visible assimilated material and is high- titanium basalt with normal chemistry. A single sample with a low titanium content (1.14 wt % TiO2; 5715A5) was collected from near the top of the stratigraphy in the Wrangell Mountains, but this sample has similar isotopic composition to the high-titanium basalts, atypical petrographic texture, and is at the upper range of TiO2 of low-titanium basalts. 7. Discussion 7.1. Source of Nikolai Basalts [29] The Nikolai Formation in Alaska has two main lava types with distinct isotopic compositions. The high-titanium basalts in Alaska have depleted Hf and Nd isotopic compositions, although they are not as depleted as most Pacific and Indian mid- ocean ridge basalts (MORB), and overlap and are displaced just below the ocean island basalt (OIB) mantle array (Figure 15). The high-titanium basalts have similar initial Sr and Nd isotopic composi- tions to Ontong Java Plateau, Hawaii, and Carib- bean Plateau basalts and similar initial eHf to Ontong Java, with slightly lower initial eHf than most Hawaii and Caribbean basalts (Figure 15). In contrast, the low-titanium basalts are displaced well above the OIB mantle array in a eHf(t)  eNd(t) correlation diagram and have higher initial eHf than age-corrected Pacific MORB at 230 Ma, with lower initial eNd than age-corrected Pacific MORB by 3 epsilon units. The Hf isotopic com- positions of the low-titanium basalts are 2 to 6 epsilon units higher than most samples from Ontong Java, which have comparable to slightly lower initial eNd. Sr isotopic compositions for low- titanium basalts extend to significantly higher ini- tial 87Sr/86Sr than Ontong Java and Hawaii. Three low-titanium basalts with particularly high initial eNd lie within a field for Indian MORB in eHf(t)  eNd(t) space. Two Rainy Creek picrite samples lie close to the eHf(t)  eNd(t) OIB mantle array with lower initial eNd than the high-titanium basalts (Figure 15). The high- and low-titanium basalts have uniform initial Pb isotopic compositions that overlap the field for Caribbean basalts and have more radiogenic initial 207Pb/204Pb than Ontong Java, Hawaii, and a field for the East Pacific Rise (EPR; Figure 15). Pb isotopic compositions for the Wrangellia basalts form a linear trend in 208Pb206Pb space that intersects the field of Pacific MORB compositions and is slightly offset toward lower 208Pb/204Pb from Ontong Java and Hawaii. The Nikolai basalts have more radiogenic Pb isotopic compositions than MORB, Ontong Figure 14. Chemostratigraphy of the Nikolai Formation in three areas of Alaska (Clearwater, Amphitheater, and Wrangell Mountains). Each column shows flow type, sample numbers, relative stratigraphic height, and TiO2 and MgO contents (in wt %). Dashed lines in each column separate individual traverses. Legend indicates flow type. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 21 of 34 Java, and OIB from Hawaii but are similar to basalts of the Caribbean Plateau. [30] The initial Hf and Nd isotopic compositions of high-titanium basalts indicate a uniform plume- type Pacific mantle source derived from a long- term depleted source, distinct from the source of MORB. In contrast, the low-titanium basalts have initial Hf isotopic compositions that are clearly distinct from OIB and initial Nd isotopic compo- sitions that are distinct from the Pacific MORB source at 230 Ma. The displacement of the low- titanium basalts well above the OIB array indicates involvement of a depleted component (mantle or crust), distinct from depleted MORB mantle, early in the formation of Nikolai basalts in Alaska. The origin of the isotopic and geochemical signature of the low-titanium basalts is the focus of subsequent discussion sections. Figure 15. Comparison of age-corrected (230 Ma) Sr-Nd-Hf-Pb isotopic compositions for Nikolai basalts in Alaska to age-corrected OIB and MORB (except for Pb plots). (a) Initial eNd versus 87Sr/86Sr. (b) Measured and initial 207Pb/204Pb versus 206Pb/204Pb. (c) Initial eHf versus eNd. (d) Measured and initial 208Pb/204Pb versus 206Pb/204Pb. References for data sources are listed in Auxiliary Material (Text S2). Most of the compiled data was extracted from the GEOROC database (http://georoc.mpch-mainz.gwdg.de/georoc/). OIB array line from Vervoort et al. [1999]. EPR is East Pacific Rise. Dashed lines indicate Bulk Silicate Earth (BSE). Estimation of fields for age-corrected Pacific MORB and EPR at 230 Ma were made using parent-daughter concentrations (in ppm) from Salters and Stracke [2004] of Lu = 0.063, Hf = 0.202, Sm = 0.27, Nd = 0.71, Rb = 0.086, and Sr = 8.36. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 22 of 34 7.2. Lithospheric Involvement in Derivation of the Low-Titanium Basalts [31] The stratigraphic relationship of the two con- trasting lava types in the Nikolai Formation pre- serves a record of a shift in composition and provides a rare opportunity to evaluate the role of oceanic arc lithosphere in the formation of an oceanic plateau. Thus far, the low-titanium basalts have primarily been recognized in the lowermost part of the stratigraphy in the western part of Wrangellia in Alaska, where there is a substantial section of submarine flows (500 m). The low- titanium basalts have the complete subduction- zone trace element signature; they have distinct negative-HFSE anomalies (Nb-Ta and Zr -Hf) and are enriched in LILE. The low-titanium basalts also have Hf-Sr-Nd isotopic compositions that are in- dicative of a component characterized by high Rb/ Sr, low Sm/Nd, and high Lu/Hf; they have high initial eHf and high initial 87Sr/86Sr compared to the high-titanium basalts. This compositional and stratigraphic evidence suggests involvement of the Paleozoic arc lithosphere in the generation of early erupted low-titanium basalts in the Wrangel- lia oceanic plateau of Alaska. 7.2.1. Nature of Underlying Paleozoic Arc Lithosphere [32] The Paleozoic arc (320–285 Ma) and marine sedimentary sequences (Early Permian to Middle Triassic) exposed beneath the Nikolai basalts in Alaska are >2.5 km thick in areas [e.g., Nokleberg et al., 1985]. Recent geophysical studies in south- ern Alaska by Saltus et al. [2007] indicate Wran- gellia crust is at least 50 km thick between the Denali and Border Ranges Faults (Figure 1). The arc crust that the Wrangellia oceanic plateau was built upon may have been 20–30 km thick and presumably included a substantial subarc lithospheric mantle that was metasomatized during arc activity. [33] In the Alaska Range, the Nikolai basalts are underlain, in decreasing order of depth, by the Paleozoic Tetelna Volcanics, the Slana Spur, and Eagle Creek Formations. Tetelna Volcanics (<1000 m) are andesitic and dacitic flows, tuffs interbedded with volcaniclastic rocks, and debris flow deposits; the Slana Spur Formation (1400 m) is marine volcaniclastics, with lesser limestone and sandstone; and the Eagle Creek Formation (900 m) is Permian argillite and limestone [Nokleberg et al., 1985]. Numerous comagmatic intermediate to felsic plutonic rocks intrude Tetelna Volcanics and the Slan Spur Formation [Nokleberg et al., 1994]. In the Wrangell Mountains, the Paleozoic sequences include the Station Creek For- mation (1200 m of mostly basaltic and andesitic flows and 800 m of volcaniclastic sequences) and the sedimentary Hasen Creek Formation (500 m of chert, black shale, sandstone, bioclastic lime- stone, and conglomerate) [Smith and MacKevett, 1970; Figure 2]. The late Paleozoic arc sequences beneath the Nikolai basalts in Alaska predate erup- tion of the Nikolai basalts by 55–90 Ma. They represent an extinct island arc assemblage that existed in the eastern Panthalassic Ocean in the late Paleozoic to Middle Triassic and formed the sub- strate upon which the Nikolai basalts were emplaced. 7.2.2. Implications of Trace Element and Isotopic Constraints [34] The trace element and isotopic compositions of the early erupted low-titanium basalts are not typical of OIB and indicate involvement of a HFSE-depleted component that was different than the plume-type source of the high-titanium basalts. The arc lithosphere is a key suspect for derivation of the low-titanium basalts because (1) the geo- chemical and isotopic signature of the low-titanium basalts has very similar characteristics to rocks formed in subduction settings [e.g., Kelemen et al., 2003]; (2) arc crust is exposed beneath the Nikolai basalts in Alaska; and (3) the low-titanium basalts only form 10–15% of the lowest part of the volcanic stratigraphy. [35] Figure 16 highlights differences in trace ele- ments and isotopic compositions between the high- and low-titanium basalts. The high-titanium basalts form a concentrated cluster of points in each of the plots and show a remarkably small degree of variation, whereas the low-titanium basalts have a noticeably wider range of variation, which mostly does not overlap the range for the high-titanium basalts (Figure 16). The low-titanium basalts have low Nb/Th and Nb/La relative to primitive mantle, which is characteristic of subduction-related rocks [Pearce, 1982]. Except for three samples from the basal flow in the Amphitheater Mountains, which has pelagic sediment between pillow tubes de- rived from the directly underlying strata and has similar Nb/Th to the high-titanium basalts, the low-titanium basalts have similar Nb/Th and Nb/La to accreted arc crust from the Early Jurassic Talk- eetna arc exposed in southern Alaska 50 km south of the Amphitheater Mountains [Greene et al., 2006; Figure 16]. Low Nb/Th in arc magmas is Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 23 of 34 Figure 16. Trace element ratios and isotopic compositions of the Nikolai Formation in Alaska. (a) 176Lu/177Hf versus Nb/Th. (b) Initial eNd versus Nb/Th. (c) Initial eHf versus Nd/Zr. (d) Zr/Nb versus Y/Nb. (e) Initial eHf versus Nb/La. (f) Initial eHf versus Sr/Nd. Primitive mantle (PM) from McDonough and Sun [1995], depleted mantle (DM) from Salters and Stracke [2004]. Talkeetna arc lower crust compositions from Greene et al. [2006] and Talkeetna arc lavas from Clift et al. [2005]. Dashed circles outline samples 5727A2, 5727A3, and 5802A5. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 24 of 34 commonly attributed to inheritance from subducted sediments [e.g., Kelemen et al., 2003]. Low Nb/La may be related to a process whereby migration of REE intomagma takes place, but mobilization of Nb is inhibited, such as by reaction between magmas and metasomatized peridotite [e.g., Kelemen et al., 1990; Kelemen et al., 1993]. The low-titanium basalts have high Sr/Nd and Nd/Zr relative to primitive mantle and the high-titanium basalts (Figure 16). Elevated Sr relative to REE may indicate addition of Sr to arc lithosphere through aqueous fluids, since Sr is more soluble than REE at high pressure [e.g., Johnson and Plank, 1999] or addition from Sr-enriched cumulates from gabbroic lower crust [e.g., Kelemen et al., 2003]. The trace element patterns of the low-titanium basalts have sizable Sr peaks, and negative Nb-Ta and Zr-Hf anomalies, that closely resemble those of gabbroic rocks formed in the lower crust of island arcs (e.g., Early Jurassic Talkeetna arc [Greene et al., 2006]). [36] Figure 17 utilizes proxies described by Pearce [2008] for identifying lithospheric input (Th-Nb) and assessing depth of melting (Ti-Yb). For the Th- Nb proxy, all the high-titanium basalts lie within a diagonal MORB-OIB array parallel to a melting vector, whereas most of the low-titanium basalts are displaced above the array, oblique to the melting vector. The low-titanium basalts follow a trend for lavas that have a subduction component, or have interacted with continental crust, and they are consistent with a relatively small amount of assimilation (F > 0.9; F is melt fraction) combined with fractional crystallization (AFC) as shown by the modeling curve of Pearce [2008; Figure 17]. A Nb-Th-depleted component is indicated for the low-titanium basalts, which also have similar Nb- Th to Talkeetna arc lavas and lower crust. For the Ti-Yb proxy, high Ti/Yb ratios for high-titanium basalts indicate residual garnet from melting at high pressure, within the OIB melting array, where- as low-titanium basalts lie along a complementary mantle melt depletion trend, similar to composi- tions of Talkeetna arc lavas [Pearce, 2008]. [37] The geochemical and isotopic results for the low-titanium basalts from this study support the hypothesis for involvement of a component de- rived from subarc lithospheric mantle. Lassiter et al. [1995] suggested a minor role for the arc lithosphere in formation of the Nikolai basalts based on a suite of nine samples from the Wrangell Mountains in Alaska. They inferred that assimila- tion of low eNd, low Nb/Th arc material may have affected the composition of the Wrangellia basalts, but that mixing of MORB mantle with low eNd arc material did not reproduce the trends in the Wran- gellia basalts. Rather, Lassiter et al. [1995] sug- gested mixing of a plume-type source, with eNd = +6 to +7, with arc material with low Nb/Th could reproduce variations in the Wrangellia flood basalts. They noted that the absence of low Nb/ La ratios in flood basalts from their data set suggests a restricted amount of lithospheric in- volvement. The lower FeO content for most of the low-titanium basalts also may reflect melting generated from refractory arc lithosphere [Lassiter and DePaolo, 1997]. [38] The low-titanium basalts may have developed an arc-type signature by melting of subduction- modified mantle, interaction of plume-derived melts with melts or material derived from the arc lithospheric, and/or reaction of magmas and meta- somatized arc peridotite early in generation of the Nikolai basalts. All CFBs show compositional evidence of involvement of lithospheric mantle or continental crust in parts of their volcanic stratig- raphy [e.g., Saunders et al., 1992]. Several CFBs and volcanic rifted margins show a transition in the eruptive sequence from a lithospheric to a plume- derived signature (e.g., Siberia [Wooden et al., 1993]; Parana [Peate and Hawkesworth, 1996]; North Atlantic Igneous Province [Kerr, 1994]; Ethiopia [Pik et al., 1999]) and a number of influ- ential studies have examined the role of plume- lithosphere interactions in the formation of flood basalt provinces [e.g., Arndt and Christensen, 1992; Menzies, 1992; Saunders et al., 1992; Turner et al., 1996; Lassiter and DePaolo, 1997]. White and McKenzie [1995] presented geochemical evidence for continental lithospheric contribution to flood basalts but indicated that the conduction of heat to the lithosphere from the plume is too slow to produce large volumes of magma in short time- spans. Arndt and Christensen [1992] found that >96% of melt in CFBs comes from the astheno- sphere and only minor amounts of melt (<5%) may originate in the lithosphere. Although there are conflicts with anhydrous melting models for the lithosphere, Lassiter and DePaolo [1997] found evidence for lithospheric mantle melting and typi- cally these melts are more abundant during early phases of flood volcanism, as they usually represent a minor volume (10–20%) of the eruptive sequen- ces (e.g., Siberia). Pik et al. [1999] proposedmelting of a shallow-level, depleted source for low-titanium basalts from Ethiopia, with a strong, but variable, lithospheric contribution. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 25 of 34 [39] For certain conditions (e.g., lithospheric thickness, duration of heating, and temperature), modeling predicts that small volumes of litho- sphere-derived basalts may be overlain by larger volumes of asthenospheric basalts [Turner et al., 1996], as is the case for Wrangellia basalts in Alaska. Turner et al. [1996] concluded that the lithospheric mantle can contribute melt if it is less than 100 km thick and if the solidus is lowered from addition of volatiles at some time in the past. Saunders et al. [1992] suggested that, although conduction alone may not cause melting of the lithosphere, rifting, and decompression, the pres- ence of hydrous phases in subcontinental litho- spheric mantle [e.g., Gallagher and Hawkesworth, 1992], melt injection from the plume into the lithosphere, and thermal and mechanical erosion of the lithosphere may all facilitate melting. Numer- ical modeling of d’Acremont et al. [2003] involving plume head-lithosphere interaction and the forma- tion of oceanic plateaus indicates thermal weaken- ing may be less important than mechanical weakening at timescales of plume head flattening and related strain rates. Farnetani and Richards [1994] found from numerical modeling, partly applied to Triassic Wrangellia stratigraphy that without extension, melting would likely be entirely sublithospheric; however, they note that they did not examine complexities of arc lithosphere and the presence of hydrous phases that would enhance melting. Although primary hydrous phases are not present in the low-titanium basalts, their origin may have involved melting of subarc lithospheric man- tle prior to thinning of the lithosphere or from mechanical or thermal erosion of the base of the lithosphere. 7.2.3. Origin of Decoupled Hf and Nd Isotopes of Low-Titanium Basalts [40] The initial Hf isotopic compositions of the low-titanium basalts indicate involvement of a component that evolved with high Lu/Hf over time but not corresponding high Sm/Nd. Parent isotopes 176Lu and 147Sm are more compatible during melting than their daughter isotopes 176Hf and 143Nd, respectively [Salters and White, 1998], and show a close coupling in the crust-mantle system; when plotting Hf versus Nd isotopes they Figure 17. Th-Nb and Ti-Yb proxies of the Nikolai Formation in Alaska with data compilation and modeling results from Pearce [2008]. (a) Th/Yb versus Nb/Yb. MORB-OIB array and assimilation-fractional crystallization (AFC) model from Pearce [2008]. (b) TiO2/Yb versus Nb/Yb. Talkeetna arc lower crust from Greene et al. [2006] and Talkeetna arc lavas from Clift et al. [2005]. Mariana arc data from Pearce et al. [2007] and Woodhead et al. [2001]. The low-titanium basalts indicate a depleted source and interaction with a subduction component combined with fractional crystallization, whereas the high-titanium basalts lie within an OIB array in Figure 17b, parallel to a melting vector that indicates higher pressure melting. See Pearce [2008] for parameters of polybaric melting and assimilation-fractional crystallization (AFC) modeling. Blue line in Figure 17a represents an AFC model following the modeling of DePaolo [1981]. Red line in Figure 17b illustrates a polybaric melting trend (with changing composition of pooled melt extracted from the mantle that undergoes decompression from the solidus to the pressure marked) for high and lower mantle potential temperatures, which corresponds to representative conditions for the generation of present-day MORB and OIB [Pearce, 2008]. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 26 of 34 form the ‘‘terrestrial array’’ [e.g., Vervoort and Blichert-Toft, 1999; van de Flierdt et al., 2004; Figure 18]. A range of processes has been pro- posed to decouple Hf and Nd isotopes. Depleted lithosphere (after MORB extraction) has high Lu/ Hf and moderate Sm/Nd and can lead to decou- pling [Salters and Zindler, 1995; Salters et al., 2006]. Processes that involve zircon or garnet, which result in larger fractionation of Lu/Hf than of Sm/Nd [e.g., Patchett et al., 1984; Vervoort et al., 2000], can drive Hf and Nd isotopic composi- tions from the terrestrial array. These processes may involve pelagic sediment, ancient melt extrac- tion, or oceanic lithosphere modified by subduction [e.g., Geldmacher et al., 2003]. The subarc mantle wedge can develop high Lu/Hf, compared to Sm/ Nd, that will evolve over time to high 176Hf/177Hf relative to 143Nd/144Nd and displace compositions above the OIB array [e.g., Barry et al., 2006]. [41] The low-titanium basalts have comparable initial eHf to modern Pacific arcs (and Pacific MORB) with lower initial eNd (Figure 18) and higher initial 87Sr/86Sr (Figure 15). The processes in the mantle wedge above a subduction zone can cause a more significant decrease in 143Nd/144Nd than 176Hf/177Hf, which then evolve along a similar path to depleted compositions well above the mantle array [Kempton et al., 2002; Janney et al., 2005]. Along with high initial eHf, high initial Sr isotope ratios of the low-titanium basalts indicate involvement of a component derived from an older source with high Rb/Sr, such as subarc lithospheric mantle. Elemental fractionation in the subarc man- tle would lead to radiogenic 176Hf/177Hf and 87Sr/86Sr and less radiogenic 143Nd/144Nd and 206Pb/204Pb [e.g., Janney et al., 2005]; these are the characteristics of the low-titanium basalts. [42] A binary mixing curve between average Pa- cific arc basalt composition and pelagic sediments, from 1000 km east of the Tonga trench (DSDP site 595/596; J. D. Vervoort, personal communica- tion, 2008), in a plot of initial eHf versus eNd suggests that involvement of a pelagic sediment component with high Lu/Hf could generate high initial Hf isotopic compositions similar to those of the low-titanium basalts (Figure 18). The bulk addition of a pelagic component (<3%) that under- went radiogenic ingrowth from high Lu/Hf could explain the displacement of low-titanium basalts above the OIB mantle array from a source more depleted than that of the high-titanium basalts. The pelagic sediment component is different than the local contamination of the basal pillowed flows in the Alaska Range that contain sediment filling interpillow voids. Pelagic sediment has very high Pb contents compared to oceanic basalts, and would be expected to generate different Pb isotopic compositions in the low- and high-titanium basalts; however, the high- and low-titanium basalts have almost indistinguishable Pb isotopes. Geldmacher et al. [2003] suggested the high 207Pb/204Pb and 208Pb/204Pb diagnostic of marine sediments may not be apparent in time periods of hundreds of millions of years if relatively high U and Pb, and high U/Pb ratio, in the sediment cause rapid in- growth of 206Pb and very little in-growth of 207Pb and 208Pb (because of decay of 235U early in Earth’s history and the long half-life of 232Th compared to 238U). The trace element and isotope geochemistry of the low-titanium basalts is best explained by involvement of a subduction-modi- fied mantle component, possibly including a pe- lagic sediment component, which may have evolved with high 176Hf/177Hf (and 87Sr/86Sr) relative to 143Nd/144Nd. 8. Conclusions [43] The volcanic stratigraphy (3.5–4 km thick) of the Nikolai Formation forms an arcuate belt 450 km long in the Wrangell Mountains and Alaska Range (Amphitheater and Clearwater Mountains) in southern Alaska. These sequences formed as part of an extensive oceanic plateau in the Middle to Late Triassic during a single, short- lived phase of volcanism lasting <5 Ma. The Nikolai Formation is bounded by marine sedimen- tary sequences and uncomformably overlies late Paleozoic volcanic arc sequences. The volcanic stratigraphy is predominantly subaerial flows in Alaska but consists of 500 m of submarine flows and basal sills intruding preexisting shale in the southern Alaska Range. [44] The Nikolai Formation is composed of high- and low-titanium basalts that record a change in the source of magmas that constructed the Wrangellia oceanic plateau in Alaska. The low-titanium basalts form the lowest 400 m of volcanic stratigraphy in the Alaska Range, and the remainder of the volca- nic stratigraphy in the Alaska Range and all of the sampled stratigraphy in the Wrangell Mountains is high-titanium basalt. The geochemistry of erupted sequences of the Wrangellia oceanic plateau in Alaska allows for assessment of the different con- tributions from the preexisting lithospheric mantle and plume-type mantle. The high-titanium basalts were derived from a uniform plume-type Pacific Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 27 of 34 mantle source, with similar initial Hf and Nd isotopic ratios to Ontong Java. The low-titanium basalts involved a HFSE-depleted, high eHf com- ponent that is distinct from OIB and MORB and was only involved during the early phase of this major melting event. There is no indication of a transitional lava type in Alaska and the high- titanium basalts do not indicate significant assim- ilation or interaction of lithospheric material. [45] Whereas almost all CFBs, and at least one oceanic plateau (e.g., Kerguelen for its Cretaceous part), record involvement of continental litho- sphere, Wrangellia flood basalts in Alaska do not indicate involvement of low eNd-low eHf continen- tal material. However, the low-titanium basalts have compositions that indicate melting and/or interaction with subduction-modified lithospheric mantle was involved in their formation. A large thermal anomaly may have initiated melting in the lithospheric mantle due to conduction of heat and possibly a lower liquidus temperature from vola- tiles in the older subarc lithospheric mantle. The Figure 18. Global Hf-Nd isotope systematics with age-corrected data of the Nikolai Formation in Alaska. Data for terrestrial array are from Vervoort and Blichert-Toft [1999] and references therein. References for data sources for Pacific arcs, Fe-Mn crusts, eolian dust are listed in Auxiliary Material (Text S2). Pelagic sediment data from DSDP 595/596 provided courtesy of J. D. Vervoort (personal communication, 2008). The mixing curve shown is for mixing of pelagic sediment with arc basalt. Average pelagic sediment composition used for mixing curve is initial eHf = +5.0 ± 4.0 and initial eNd = 4.5 ± 2.4. Average arc basalt from average of Pearce et al. [2007] and Woodhead et al. [2001]. Pacific MORB from Nowell et al. [1998], Salters and White [1998], and Chauvel and Blichert-Toft [2001]. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 28 of 34 lithosphere may have been mechanically or ther- mally eroded, whereafter melting occurred mostly within the plume to produce the voluminous high- titanium basalts. Appendix A: Sample Preparation and Analytical Methods [46] The least altered samples of the Nikolai For- mation were selected for geochemical analysis based on thorough petrographic inspection. Thir- ty-seven of 68 samples from the Alaska Range and 16 of 36 samples from the Wrangell Mountains were crushed (400 g) into pieces <2 mm in diameter in a Rocklabs hydraulic piston crusher between WC plates. The coarse crush was thor- oughly mixed and 100 g was powdered in a planetary mill using agate jars and balls that were cleaned with quartz sand between samples. A1. University of Massachusetts XRF Analytical Methods [47] Fifty-three sample powders and six duplicate powders were analyzed at the Ronald B. Gilmore X-Ray Fluorescence Laboratory (XRF) at the Uni- versity of Massachusetts. Major elements were measured on a fused La-bearing lithium borate glass disc using a Siemens MRS-400 spectrometer with a Rh X-ray tube operating at 2700 W. Trace element concentrations (Rb, Sr, Ba, Ce, Nb, Zr, Y, Pb, Zn, Ga, Ni, Cr, V) were measured on a separate powder pellet using a Philips PW2400 sequential spectrometer with a Rh X-ray tube. Loss on igni- tion (LOI) and ferrous iron measurements were made as described by Rhodes and Vollinger [2004]. Precision and accuracy estimates for the analytical data are described by Rhodes [1996] and Rhodes and Vollinger [2004]. Results for each sample are the average of two separate analyses. A total of four complete duplicates were analyzed for Alaska samples. Eighteen sample duplicate powders of Wrangellia flood basalts were also analyzed at Activation Laboratories and the results for most elements were within analytical error. A2. PCIGR Trace Element and Isotopic Analytical Methods [48] A subset of 24 samples was selected for high- precision trace element analysis and Sr, Nd, Pb, and Hf isotopic analysis at the Pacific Centre for Isotopic and Geochemical Research (PCIGR) at the University of British Columbia (UBC; Table 1). Samples were selected from the 53 samples ana- lyzed by XRF, based on major and trace element chemistry, alteration (low LOI and petrographic alteration index), sample location, and stratigraphic position. Samples were prepared for trace element analysis at the PCIGR by the technique described by Pretorius et al. [2006] on unleached rock powders. Sample powders (100 mg) were weighed in 7 mL screw-top Savillex 1 beakers and dissolved in 1 mL 14N HNO3 and 5 mL 48% HF on a hotplate for 48 h at 130C with periodic ultrasonication. Samples were dried and redissolved in 6 mL 6N HCl on a hotplate for 24 h and then dried and redissolved in 1 mL concen- trated HNO3 for 24 h before final drying. Trace element abundances were measured with a Thermo Finnigan Element2 High Resolution-Inductively Coupled Plasma-Mass Spectrometer (HR-ICP- MS) following the procedures described by Pretorius et al. [2006] within 24 h of redissolu- tion. High field strength elements (HFSE) and large ion lithophile elements (LILE) were measured in medium resolution mode at 2000X dilution using a PFATeflon spray chamber washed with Aqua Regia for 3 min between samples. Rare earth elements (REE) were measured in high-resolution mode, and U and Pb were measured in low-resolution mode, at 2000X dilution using a glass spray chamber washed with 2% HNO3 between samples. Total procedural blanks and reference materials (BCR-2, BHVO-2) were analyzed with the batch of samples. Indium was used as an internal standard in all samples and standard solutions. Background and standard solu- tions were analyzed after every five samples to detect memory effects and mass drift. [49] Sample digestion for purification of Sr, Nd, Hf, and Pb for column chemistry involved weigh- ing each sample powder. All samples were initially leached with 6N HCl and placed in an ultrasonic bath for 15 min. Samples were rinsed two times with 18 mega W-cm H2O between each leaching step (15 total) until the supernatant was clear (following the technique of Mahoney [1987], mod- ified by Weis and Frey [1991]). Samples were then dried on a hotplate for 24 h and weighed again. Sample solutions were then prepared by dissolving 100–250 mg of the leached powder dissolved in 1 mL 14N HNO3 and 10 mL 48% HF on a hotplate for 48 h at 130C with periodic ultra- sonication. Samples were dried and redissolved in 6 mL 6N HCl on a hotplate for 24 h and then dried. Pb was separated using anion exchange columns and the discard was used for Sr, REE, and Hf separation. Nd was separated from the REE and Hf required two additional purification steps. Detailed Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 29 of 34 procedures for column chemistry for separating Sr, Nd, and Pb at the PCIGR are described by Weis et al. [2006] and Hf purification is described by Weis et al. [2007]. Sr and Nd isotope ratios were measured on a Thermo Finnigan Triton Thermal Ionization Mass Spectrometer (TIMS) in static mode with relay matrix rotation on a single Ta and double Re-Ta filament, respectively. Four to five filaments per barrel of 21 were occupied by standards (NIST SRM 987 for Sr and LaJolla for Nd) for each barrel where samples were run. Sample Sr and Nd isotopic compositions were corrected for mass fractionation using 86Sr/88Sr = 0.1194 and 146Nd/144Nd = 0.7219. Each sample was then normalized using the barrel average of the reference material relative to the values of 143Nd/144Nd = 0.511858 and 87Sr/86Sr = 0.710248 [Weis et al., 2006]. During the period when the Alaska samples were analyzed, the La Jolla Nd standard gave an average value of 0.511853 ± 11 (n = 8) and NIST SRM 987 standard gave an average of 0.710253 ± 11 (n = 9; 2s error is reported as times 106). 147Sm/144Nd ratio errors are approximately 1.5%, or 0.006. Leached powder of United States Geological Survey (USGS) reference material BHVO-2 was processed with the samples and yielded Sr and Nd isotopic ratios of 0.703473 ± 8 and 0.512980 ± 6, respec- tively. These are in agreement with the published values of 0.703479 ± 20 and 0.512984 ± 11, respectively [Weis et al., 2006]. USGS reference material BCR-2 was processed with the samples and yielded Sr and Nd isotopic ratios of 0.705002 ± 9 and 0.512633 ± 7, respectively, which are in agree- ment with the published values of 0.705013 ± 10 and 0.512637 ± 12, respectively [Weis et al., 2006]. [50] Pb and Hf isotopic compositions were ana- lyzed by static multicollection on a Nu Plasma (Nu Instruments) Multiple Collector-Inductively Cou- pled Plasma-Mass Spectrometer (MC-ICP-MS). The detailed analytical procedure for Pb isotopic analyses on the Nu at the PCIGR is described by Weis et al. [2005]. The configuration for Pb anal- yses allows for collection of Pb, Tl, and Hg together. Tl and Hg are used to monitor instru- mental mass discrimination and isobaric overlap, respectively. All sample solutions were analyzed with approximately the same Pb/Tl ratio (4) as the reference material NIST SRM 981. To accom- plish this, a small aliquot of each sample solution from the Pb columns was analyzed on the Ele- ment2 to determine the precise amount of Pb available for analysis on the Nu Plasma. The SRM 981 standard was run after every two samples on the Nu Plasma. During the time samples were run, analyses of the SRM 981 Pb reference material gave values of 206Pb/204Pb = 16.9403 ± 19, 207Pb/204Pb = 15.4964 ± 20, and 208Pb/204Pb = 36.7142 ± 53 (n = 124; 2s error is reported as times 104); these values are in excel- lent agreement with reported TIMS triple-spike values of Galer and Abouchami [1998]. Results were further corrected by the sample-standard bracketing method or the ln-ln correction method described by White et al. [2000] and Blichert-Toft et al. [2003]. Leached powder of USGS reference material BHVO-2 yielded Pb isotopic ratios of 206Pb/204Pb = 18.6500 ± 7, 207Pb/204Pb = 15.5294 ± 7, and 208Pb/204Pb = 38.2380 ± 19. These values are in agreement with leached resi- dues of BHVO-2 from Weis et al. [2006]. [51] Hf isotopic compositions were analyzed fol- lowing the procedures detailed by Weis et al. [2007]. The configuration for Hf analyses moni- tored Lu mass 175 and Yb mass 172 to allow for interference correction to masses 174 and 176. Hf isotopic ratios were normalized internally for mass fractionation to a 179Hf/177Hf ratio of 0.7325 using an exponential correction. Standards were run after every two samples and sample results were nor- malized to the ratio of the in-run daily average and a 176Hf/177Hf ratio for JMC-475 of 0.282160. During the course of analyses, the Hf standard JMC-475 gave an average value 0.282153 ± 3 (n = 79). USGS reference materials BCR-2 and BHVO-2 were processed with the samples and yielded Hf isotopic ratios of 0.282874 ± 5 and 0.283114 ± 6, respectively. Published values for BCR-2 and BHVO-2 are 0.282871 ± 7 and 0.283104 ± 8, respectively [Weis et al., 2007]. Acknowledgments [52] We are grateful to Jeff Trop and Danny Rosenkrans for their advice on geology and logistics within Wrangell-St. Elias National Park. Jeanine Schmidt was very helpful with field advice and information about Wrangellia geology. We also appreciate insights from Jeff Vervoort and Julian Pearce and thank Nick Arndt for inspiring this study. Bruno Kieffer and Jane Barling assisted with some analytical work. Reviews by Vincent Salters, Andrew Kerr, John Mahoney, and Barry Hanan are greatly appreciated. Funding was provided by NSERC Discovery Grants to J. Scoates and D. Weis. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 30 of 34 A. Greene was supported by a University Graduate Fellowship at UBC. References Armstrong, A. K., and E. M. MacKevett Jr. (1977), The Trias- sic Chitistone Limestone, Wrangell Mountains, Alaska, U.S. Geol. Surv. Open File Rep., 77–217, D49–D62. Armstrong, A. K., and E. M. MacKevett Jr. (1982), Stratigra- phy and diagenetic history of the lower part of the Triassic Chitistone Limestone, Alaska, U.S. Geol. Surv. Prof. Pap., 1212-A, 1–26. Arndt, N. T., and U. Christensen (1992), The role of litho- spheric mantle in continental flood volcanism: Thermal and geochemical constraints, J. Geophys. Res., 97(B7), 10,967–10,981, doi:10.1029/92JB00564. Arndt, N. T., G. K. Czamanske, and J. L. Wooden (1993), Mantle and crustal contributions to continental flood volcan- ism, Tectonophysics, 223, 39–52, doi:10.1016/0040- 1951(93)90156-E. Barry, T. L., J. A. Pearce, P. T. Leat, I. L. Millar, and A. P. le Roex (2006), Hf isotope evidence for selective mobility of high-field-strength elements in a subduction setting: South Sandwich Islands, Earth Planet. Sci. Lett., 252, 223–244, doi:10.1016/j.epsl.2006.09.034. Bittenbender, P. E., K. W. Bean, J. M. Kurtak, and J. Deninger Jr. (2007), Mineral assessment of the Delta River Mining District area, East-central Alaska, Tech. Rep. 57, U. S. Bur. of Land Manage., Anchorage, Alaska. (Available at http:// www.blm.gov/pgdata /e tc /media l ib/b lm/ak/aktes t / tr.Par.86412.File.dat/BLM_TR57.pdf) Blichert-Toft, J., D. Weis, C. Maerschalk, A. Agranier, and F. Albarède (2003), Hawaiian hot spot dynamics as inferred from the Hf and Pb isotope evolution of Mauna Kea volcano, Geochem. Geophys. Geosyst., 4(2), 8704, doi:10.1029/ 2002GC000340. Chauvel, C., and J. Blichert-Toft (2001), A hafnium isotope and trace element perspective on melting of the depleted mantle, Earth Planet. Sci. Lett., 190, 137 – 151, doi:10.1016/S0012-821X(01)00379-X. Clift, P., A. Draut, P. Kelemen, J. Blusztajn, and A. Greene (2005), Stratigraphic and geochemical evolution of the Jur- assic Talkeetna Volcanic Formation, south-central Alaska, Geol. Soc. Am. Bull., 117(7), 902–925, doi:10.1130/ B25638.1. Coffin, M. F., R. A. Duncan, O. Eldholm, J. G. Fitton, F. A. Frey, H. C. Larsen, J. J. Mahoney, A. D. Saunders, R. Schlich, and P. J. Wallace (2006), Large igneous provinces and scien- tific ocean drilling: Status quo and a look ahead, Oceano- graphy, 19(4), 150–160. Cox, K. G., R. MacDonald, and G. Hornung (1967), Geo- chemical and petrographic provinces in the Karoo basalts of southern Africa, Am. Mineral., 52, 1451–1474. d’Acremont, E., S. Leroy, and E. B. Burov (2003), Numerical modelling of a mantle plume: The plume head-lithosphere interaction in the formation of an oceanic large igneous pro- vince, Earth Planet. Sci. Lett., 206(3–4), 379–396. DePaolo, D. J. (1981), Trace element and isotopic effects of combined wallrock assimilation and fractional crystalliza- tion, Earth Planet. Sci. Lett., 53, 189–202, doi:10.1016/ 0012-821X(81)90153-9. Farnetani, C. G., and M. A. Richards (1994), Numerical in- vestigations of the mantle plume initiation model for flood basalt event, J. Geophys. Res., 99, 13,813–13,834, doi:10.1029/94JB00649. Galer, S. J. G., and W. Abouchami (1998), Practical applica- tion of lead triple spiking for correction of instrumental mass discrimination, Mineral. Mag., 62A, 491–492, doi:10.1180/ minmag.1998.62A.1.260. Gallagher, K., and C. Hawkesworth (1992), Dehydration melt- ing and the generation of continental flood basalts, Nature, 358, 57–59, doi:10.1038/358057a0. Gardner, M. C., S. C. Bergman, G. W. Cushing, E. M. MacKevett Jr., G. Plafker, R. B. Campbell, C. J. Dodds, W. C. McClelland, and P. A. Mueller (1988), Pennsylva- nian pluton stitching of Wrangellia and the Alexander ter- rane, Wrangell Mountains, Alaska, Geology, 16, 967–971, doi:10.1130/0091-7613(1988)016<0967:PPSOWA>2.3. CO;2. Geldmacher, J., B. B. Hanan, J. Blichert-Toft, K. Harpp, K. Hoernle, F. Hauff, R. Werner, and A. C. Kerr (2003), Hafnium isotopic variations in volcanic rocks from the Caribbean Large Igneous Province and Galapagos hot spot tracks, Geochem. Geophys. Geosyst., 4(7), 1062, doi:10.1029/2002GC000477. Glen, J. M. G., J. M. Schmidt, and R. Morin (2007), Gravity and magnetic studies of the Talkeetna Mountains, Alaska: Constraints on the geological and tectonic interpretation of southern Alaska, and implications for mineral exploration, in Tectonic Growth of a Collisional Continental Margin: Crus- tal Evolution of Southern Alaska, edited by K. D. Ridgway et al., Geol. Soc. Am. Spec. Pap., 431, 593–622. Greene, A. R., S. M. DeBari, P. B. Kelemen, J. Blusztajn, and P. D. Clift (2006), A detailed geochemical study of island arc crust: The Talkeetna Arc section, south-central Alaska, J. Petrol., 47(6), 1051–1093, doi:10.1093/petrology/egl002. Greene, A. R., J. S. Scoates, D. Weis, and S. Israel (2008a), Geochemistry of flood basalts from the Yukon (Canada) seg- ment of the accreted Wrangellia oceanic plateau, Lithos, in press. Greene, A. R., J. S. Scoates, D. Weis, G. T. Nixon, and B. Kieffer (2008b), Magmatic history and growth of the accreted Wrangellia oceanic plateau on Vancouver Island, Canada, J. Petrol, in press. Hooper, P. R., and C. J. Hawkesworth (1993), Isotopic and geochemical constraints on the origin and evolution of the Columbia River Basalt, J. Petrol., 34(6), 1203–1246. Hornig, I. (1993), High-Ti and low-Ti tholeiites in the Jurassic Ferrar Group, Antarctica, Geol. Jahrb., Reihe E Geophys., 47, 335–369. Janney, P. E., A. P. Le Roex, and R. W. Carlson (2005), Haf- nium isotope and trace element constraints on the nature of mantle heterogeneity beneath the Central Southwest Indian Ridge (13E to 47E), J. Petrol., 46(12), 2427–2464, doi:10.1093/petrology/egi060. Johnson, M. C., and T. Plank (1999), Dehydration and melting experiments constrain the fate of subducted sediments, Geo- chem. Geophys. Geosyst., 1(1), 1007, doi:10.1029/ 1999GC000014. Jones, D. L., N. J. Silberling, and J. Hillhouse (1977), Wran- gellia; a displaced terrane in northwestern North America, Can. J. Earth Sci., 14(11), 2565–2577. Kelemen, P. B., K. T. M. Johnson, R. J. Kinzler, and A. J. Irving (1990), High-field-strength element depletions in arc basalts due to mantle-magma interaction, Nature, 345, 521– 524, doi:10.1038/345521a0. Kelemen, P. B., N. Shimizu, and T. Dunn (1993), Relative depletion of niobium in some arc magmas and the continen- tal crust: Partitioning of K, Nb, La and Ce during melt/rock reaction in the upper mantle, Earth Planet. Sci. Lett., 120, 111–134, doi:10.1016/0012-821X(93)90234-Z. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 31 of 34 Kelemen, P. B., K. Hanghøj, and A. R. Greene (2003), One view of the geochemistry of subduction-related magmatic arcs, with emphasis on primitive andesite and lower crust, in The Crust, edited by R. Rudnick, pp. 593–659, Elsevier, Oxford, U. K. Kempton, P. D., J. A. Pearce, T. L. Barry, J. G. Fitton, C. H. Langmuir, and D. M. Christie (2002), Sr-Nd-Pb-Hf isotope results from ODP Leg 187: Evidence for mantle dynamics of the Australian-Antarctic Discordance and origin of the In- dian MORB source, Geochem. Geophys. Geosyst., 3(12), 1074, doi:10.1029/2002GC000320. Kerr, A. C. (1994), Lithospheric thinning during the evolution of continental large igneous provinces: A case study from the North Atlantic Tertiary province, Geology, 22, 1027–1030, doi:10.1130/0091-7613(1994)022<1027:LTDTEO>2.3. CO;2. Kerr, A. C., and J. J. Mahoney (2007), Oceanic plateaus: Pro- blematic plumes, potential paradigms, Chem. Geol., 241, 332–353, doi:10.1016/j.chemgeo.2007.01.019. Lassiter, J. C. (1995), Geochemical investigations of plume- related lavas: Constraints on the structure of mantle plumes and the nature of plume/lithosphere interactions, Ph.D. dis- sertation, 231 pp., Univ. of Calif., Berkeley. Lassiter, J. C., and D. J. DePaolo (1997), Plume/lithosphere inter- action in the generation of continental and oceanic flood basalts: Chemical and isotopic constraints, in Large Igneous Provinces: Continental, Oceanic, and Planetary Flood Volcanism, Geo- phys. Monogr. Ser., vol. 100, edited by J. J. Mahoney and M. F. Coffin, pp. 335–355, AGU, Washington, D. C. Lassiter, J. C., D. J. DePaolo, and J. J. Mahoney (1995), Geo- chemistry of the Wrangellia flood basalt province: Implica- tions for the role of continental and oceanic lithosphere in flood basalt genesis, J. Petrol., 36(4), 983–1009. MacDonald, G. A., and T. Katsura (1964), Chemical composi- tion of Hawaiian lavas, J. Petrol., 5, 82–133. MacKevett, E. M., Jr. (1978), Geologic map of the McCarthy Quadrangle, Alaska, U.S. Geol. Surv. Misc. Geol. Invest.Map I-1032, scale 1:250,000. MacKevett, E.M., Jr., D. P. Cox,R. P. Potter, andM. L. Silberman (1997), Kennecott-type deposits in the Wrangell Mountains, Alaska:High-grade copper ores near a basalt-limestone contact, in Mineral Deposits of Alaska, Econ. Geol. Monogr., vol. 9, edited by R. J. Goldfarb and L. D. Miller, pp. 66–89, Econ. Geol. Publ., Lancaster, Pa. Mahoney, J. J. (1987), An isotopic survey of Pacific oceanic plateaus: Implications for their nature and origin, in Sea- mounts, Islands, and Atolls, Geophys. Monogr. Ser., vol. 43, edited by B. H. Keating et al., pp. 207–220, AGU, Washington, D. C. McDonough, W. F., and S. Sun (1995), The composition of the Earth, Chem. Geol., 120, 223–253, doi:10.1016/0009- 2541(94)00140-4. Melluso, L., L. Beccaluva, P. Brotzu, A. Gregnanin, A. K. Gupta, L. Morbidelli, and G. Traversa (1995), Constraints on the mantle sources of the Deccan Traps from the petrol- ogy and geochemistry of the basalts of Gujarat State (Wes- tern India), J. Petrol., 36(5), 1393–1432, doi:10.1093/ petrology/36.5.1393. Menzies, M. A. (1992), The lower lithosphere as a major source for continental flood basalts: A re-appraisal, in Mag- matism and the Causes of Continental Break-up, edited by B. C. Storey, T. Alabaster, and R. J. Pankhurst, Geol. Soc. Spec. Publ., 68, 31–39. Nobre Silva, I. G., D. Weis, J. Barling, and J. S. Scoates (2008), Leaching systematics for the determination of high- precision Pb isotope compositions of ocean island basalts, Geochem. Geophys. Geosyst., doi:10.1029/2007GC001891, in press. Nokleberg, W. J., D. L. Jones, and N. J. Silberling (1985), Origin and tectonic evolution of the Maclaren and Wrangel- lia terranes, eastern Alaska Range, Alaska, Geol. Soc. Am. Bull., 96, 1251 –1270, doi:10.1130/0016-7606(1985) 96<1251:OATEOT>2.0.CO;2. Nokleberg, W. J., J. N. Aleinikoff, J. T. J. Dutro, M. A. Lanphere, N. J. Silberling, S. R. Silva, T. E. Smith, and D. L. Turner (1992), Map, tables, and summary fossil and isotopic age data, Mount Hayes quadrangle, eastern Alaska Range, Alaska, U.S. Geol. Surv. Misc. Field Stud.Map, 1996-D, scale. 1:250,000. Nokleberg, W. J., G. Plafker, and F. H. Wilson (1994), Geol- ogy of south-central Alaska, in The Geology of North Amer- ica, edited by G. Plafker and H. C. Berg, pp. 311–366, Geol. Soc. of Am., Boulder, Colo. Nomade, S., A. Pouclet, and Y. Chen (2002), The French Guyana doleritic dykes: Geochemical evidence of three po- pulations and new data for the Jurassic Central Atlantic Mag- matic Province, J. Geodyn., 34(5), 595–614, doi:10.1016/ S0264-3707(02)00034-0. Nowell, G. M., P. D. Kempton, S. R. Noble, J. G. Fitton, A. Saunders, J. J. Mahoney, and R. N. Taylor (1998), High precision Hf isotope measurements of MORB and OIB by thermal ionisation mass spectrometry: Insights into the depleted mantle, Chem. Geol., 149, 211–233, doi:10.1016/S0009-2541(98)00036-9. Patchett, P. J., W. M. White, H. Feldmann, S. Kielinczuk, and A. W. Hofmann (1984), Hafnium/rare earth element fractio- nation in the sedimentary system and crustal recycling into the Earth’s mantle, Earth Planet. Sci. Lett., 69, 365–378, doi:10.1016/0012-821X(84)90195-X. Pearce, J. A. (1982), Trace element characteristics of lavas from destructive plate boundaries, in Andesites: Orogenic Andesites and Related Rocks, edited by R. S. Thorpe, pp. 526–547, John Wiley, Chichester, U. K. Pearce, J. A. (2008), Geochemical fingerprinting of oceanic basalts with applications to ophiolite classification and the search for Archean oceanic crust, Lithos, 100, 14–48, doi:10.1016/j.lithos.2007.06.016. Pearce, J. A., P. D. Kempton, and J. B. Gill (2007), Hf-Nd evidence for the origin and distribution of mantle domains in the SW Pacific, Earth Planet. Sci. Lett., 260, 98–114, doi:10.1016/j.epsl.2007.05.023. Peate, D. W. (1997), The Parana-Etendeka Province, in Large Igneous Provinces: Continental, Oceanic, and Planetary Flood Volcanism, Geophys. Monogr. Ser., vol. 100, edited by M. F. Coffin and J. Mahoney, pp. 217–245, AGU, Washington, D. C. Peate, D. W., and C. Hawkesworth (1996), Lithospheric to asthenospheric transition in low-Ti flood basalts from south- ern Parana, Brazil, Chem. Geol., 127, 1–24, doi:10.1016/ 0009-2541(95)00086-0. Pik, R., C. Deniel, C. Coulon, G. Yirgu, C. Hofmann, and D. Ayalew (1998), The northwestern Ethiopian Plateau flood basalts: Classification and spatial distribution of magma types, J. Volcanol. Geotherm. Res., 81, 91–111, doi:10.1016/S0377-0273(97)00073-5. Pik, R., C. Deniel, C. Coulom, G. Yirgu, and B. Marty (1999), Isotopic and trace element signatures of Ethiopian flood ba- salts: Evidence for plume-lithosphere interaction, Geochim. Cosmochim. Acta, 63, 2263–2279, doi:10.1016/S0016- 7037(99)00141-6. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 32 of 34 Plafker, G., W. J. Nokleberg, and J. S. Lull (1989), Bedrock geology and tectonic evolution of the Wrangellia, Peninsular, and Chugach terranes along the Trans-Alaskan Crustal Transect in the northern Chugach Mountains and southern Copper River basin, Alaska, J. Geophys. Res., 94, 4255– 4295, doi:10.1029/JB094iB04p04255. Plafker, G., J. C. Moore, and G. R. Winkler (1994), Geology of the southern Alaska margin, in The Geology of North Amer- ica, edited by G. Plafker and H. C. Berg, pp. 389–449, Geol. Soc. of Am., Bouler, Colo. Pretorius, W., D. Weis, G. Williams, D. Hanano, B. Kieffer, and J. S. Scoates (2006), Complete trace elemental charac- terization of granitoid (USGSG-2,GSP-2) reference materials by high resolution inductively coupled plasma-mass spectro- metry, Geostand. Geoanal. Res., 30(1), 39–54, doi:10.1111/ j.1751-908X.2006.tb00910.x. Rhodes, J. M. (1996), Geochemical stratigraphy of lava flows sampled by the Hawaii Scientific Drilling Project, J. Geo- phys. Res., 101(B5), 11,729 – 11,746, doi:10.1029/ 95JB03704. Rhodes, J. M., and M. J. Vollinger (2004), Composition of basaltic lavas sampled by phase-2 of the Hawaii Scientific Drilling Project: Geochemical stratigraphy and magma types, Geochem. Geophys. Geosyst., 5, Q03G13, doi:10.1029/ 2002GC000434. Richards, M. A., D. L. Jones, R. A. Duncan, and D. J. DePaolo (1991), A mantle plume initiation model for the Wrangellia flood basalt and other oceanic plateaus, Science, 254, 263– 267, doi:10.1126/science.254.5029.263. Richter, D. H., J. G. Smith, M. A. Lanphere, G. B. Dalrymphe, B. L. Reed, and N. Shew (1990), Age and progression of volcanism, Wrangell volcanic field, Alaska, Bull. Volcanol., 53, 29–44, doi:10.1007/BF00680318. Rioux, M., B. Hacker, J. Mattinson, P. Kelemen, J. Blusztajn, and G. Gehrels (2007), Magmatic development of an intra- oceanic arc: High-precision U-Pb zircon and whole-rock iso- topic analyses from the accreted Talkeetna arc, south-central Alaska, Geol. Soc. Am. Bull., 119, 1168–1184, doi:10.1130/ B25964.1. Salters, V. J. M., and A. Stracke (2004), Composition of the depleted mantle, Geochem. Geophys. Geosyst., 5, Q05B07, doi:10.1029/2003GC000597. Salters, V. J., and W. White (1998), Hf isotope constraints on mantle evolution, Chem. Geol., 145, 447–460, doi:10.1016/ S0009-2541(97)00154-X. Salters, V. J. M., and A. Zindler (1995), Extreme 176Hf/177Hf in the sub-oceanic mantle, Earth Planet. Sci. Lett., 129, 13– 30, doi:10.1016/0012-821X(94)00234-P. Salters, V., J. Blichert-Toft, Z. Fekiacova, A. Sachi-Kocher, and M. Bizimis (2006), Isotope and trace element evidence for depleted lithosphere in the source of enriched Ko’olau basalts, Contrib. Mineral. Petrol., 151(3), 297–312, doi:10.1007/s00410-005-0059-y. Saltus, R. W., T. Hudson, and F. H. Wilson (2007), The geophy- sical character of southern Alaska: Implications for crustal evolution, in Tectonic Growth of a Collisional Continental Margin: Crustal Evolution of Southern Alaska, edited by K. D. Ridgeway et al., Geol. Soc. Am. Spec. Pap., 431, 1–20. Saunders, A. D. (2005), Large igneous provinces: Origin and environmental consequences, Elements, 1, 259–263, doi:10.2113/gselements.1.5.259. Saunders, A. D., M. Storey, R. W. Kent, and M. J. Norry (1992), Consequences of plume-lithosphere interactions, in Magmatism and the Causes of Continental Breakup, edited by B. C. Storey, T. Alabaster, and R. J. Pankhurst, Geol. Soc. London Spec. Publ., 68, 41–60. Schmidt, J. M., and R. K. Rogers (2007), Metallogeny of the Nikolai large igneous province (LIP) in southern Alaska and its influence on the mineral potential of the Talkeetna Moun- tains, in Tectonic Growth of a Collisional Continental Mar- gin: Crustal Evolution of Southern Alaska, edited by K. D. Ridgway et al., Geol. Soc. Am. Spec. Pap., 431, 623–648. Smith, J. G., and E. M. MacKevett Jr. (1970), The Skolai Group in the McCarthy B-4, C-4, C-5 Quadrangles, Wrangell Moun- tains, Alaska, U.S. Geol. Surv. Bull., 1274-Q, Q1–Q26. Smith, T. E. (1981), Geology of the Clearwater Mountains, south central Alaska, Geol. Rep. 60, 72 pp., Alaska Div. of Geol. and Geophys. Surv., Fairbanks, Alaska. Stout, J. H. (1976), Geology of the Eureka Creek area, east- central Alaska Range, Geol. Rep. 46, 32 pp., Alaska Div. of Geol. and Geophys. Surv., Fairbanks. Thompson, P. M. E., P. D. Kempton, and A. C. Kerr (2008), Evaluation of the effects of alteration and leaching on Sm-Nd and Lu-Hf systematics in submarine mafic rocks, Lithos, 104, 164–176, doi:10.1016/j.lithos.2007.12.005. Turner, S., C. Hawkesworth, K. Gallagher, K. Stewart, D. Peate, and M. Mantovani (1996), Mantle plumes, flood ba- salts, and thermal models for melt generation beneath con- tinents: Assessment of a conductive heating model and application to the Paraná, J. Geophys. Res., 101(B5), 11,503–11,518, doi:10.1029/96JB00430. van de Flierdt, T., M. Frank, D.-C. Lee, A. N. Halliday, B. C. Reynolds, and J. R. Hein (2004), New constraints on the sources and behavior of neodymium and hafnium in sea- water from Pacific Ocean ferromanganese crusts, Geochim. Cosmochim. Acta, 68(19), 3827–3843, doi:10.1016/ j.gca.2004.03.009. Vervoort, J. D., and J. Blichert-Toft (1999), Evolution of the depleted mantle: Hf isotope evidence from juvenile rocks through time, Geochim. Cosmochim. Acta, 63, 533–556, doi:10.1016/S0016-7037(98)00274-9. Vervoort, J. D., P. J. Patchett, J. Blichert-Toft, and F. Albarède (1999), Relationships between Lu-Hf and Sm-Nd isotopic systems in the global sedimentary system, Earth Planet. Sci. Lett., 168, 79–99, doi:10.1016/S0012-821X(99)00047-3. Vervoort, J. D., P. J. Patchett, F. Albarède, J. Blichert-Toft, R. L. Rudnick, and H. Downes (2000), Hf-Nd isotopic evolution of the lower crust, Earth Planet. Sci. Lett., 181, 115–129, doi:10.1016/S0012-821X(00)00170-9. Weis, D., and F. A. Frey (1991), Isotope geochemistry of the Ninetyeast Ridge basement basalts: Sr, Nd, and Pb evidence for involvement of the Kerguelen hot spot, in Proceedings of the Ocean Drilling Program, Scientific Results, edited by J. Weissel et al., pp. 591–610, Ocean Drill. Program, Col- lege Station, Tex. Weis, D., B. Kieffer, C. Maerschalk, W. Pretorius, and J. Barling (2005), High-precision Pb-Sr-Nd-Hf isotopic characterization of USGS BHVO-1 and BHVO-2 reference materials, Geo- chem. Geophys. Geosyst., 6, Q02002, doi:10.1029/ 2004GC000852. Weis, D., et al. (2006), High-precision isotopic characterization of USGS reference materials by TIMS and MC-ICP-MS, Geochem. Geophys. Geosyst., 7, Q08006, doi:10.1029/ 2006GC001283. Weis, D., B. Kieffer, D. Hanano, I. N. Silva, J. Barling, W. Pretorius, C. Maerschalk, and N. Mattielli (2007), Hf isotope compositions of U.S. Geological Survey reference materials, Geochem. Geophys. Geosyst., 8, Q06006, doi:10.1029/ 2006GC001473. White, R. S., and D. McKenzie (1995), Mantle plumes and flood basalts, J. Geophys. Res., 100, 17,543–17,585, doi:10.1029/95JB01585. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 33 of 34 White, W. M., F. Albarède, and P. Télouk (2000), High- precision analysis of Pb isotope ratios by multi-collector ICP-MS, Chem. Geol., 167, 257–270, doi:10.1016/S0009- 2541(99)00182-5. Wilson, F. H., J. D. Dover, D. C. Bradley, F. R. Weber, T. K. Bundtzen, and P. J. Haeussler (1998), Geologicmap of Central (Interior) Alaska, U.S. Geol. Surv. Open File Rep., 98-133-A. (Available at http://wrgis.wr.usgs.gov/open-file/of98-133-a/) Wilson, F. H., K. A. Labay, N. B. Shew, C. C. Preller, S. Mohadjer, and D. H. Richter (2005), Digital Data for the Geology of Wrangell-Saint Elias National Park and Pre- serve, Alaska, U.S. Geol. Surv. Open File Rep., 2005–1342. (Available at http://pubs.usgs.gov/of/2005/1342/) Wooden, J. L., G. K. Czamanske, V. A. Fedorenko, N. T. Arndt, C. Chauvel, R. M. Bouse, B. S. W. King, R. J. Knight, and D. F. Siems (1993), Isotopic and trace-element constraints on mantle and crustal contributions to Siberian continental flood basalts, Noril’sk area, Siberia, Geochim. Cosmochim. Acta, 57, 3677–3704, doi:10.1016/0016- 7037(93)90149-Q. Woodhead, J. D., J. M. Hergt, J. P. Davidson, and S. M. Eggins (2001), Hafnium isotope evidence for ‘conservative’ element mobility during subduction zone processes, Earth Planet. Sci. Lett., 192, 331–346, doi:10.1016/S0012-821X(01) 00453-8. Xu, Y., S. L. Chung, B.-M. Jahn, and G. Wu (2001), Petrologic and geochemical constraints on the petrogenesis of Permian- Triassic Emeishan flood basalts in southwestern China, Lithos, 58, 145–168, doi:10.1016/S0024-4937(01)00055-X. Geochemistry Geophysics Geosystems G3 greene et al.: wrangellia flood basalts in alaska 10.1029/2008GC002092 34 of 34

Cite

Citation Scheme:

    

Usage Statistics

Country Views Downloads
China 7 28
France 5 0
United States 5 0
Sweden 2 0
Canada 1 0
City Views Downloads
Beijing 7 0
Unknown 5 0
Ashburn 4 0
Stockholm 2 0
Mountain View 1 0
Vancouver 1 0

{[{ mDataHeader[type] }]} {[{ month[type] }]} {[{ tData[type] }]}

Share

Share to:

Comment

Related Items