Frontiers reaches 6.4 on Journal Impact Factors

Original Research ARTICLE

Front. Earth Sci., 07 July 2016 | https://doi.org/10.3389/feart.2016.00073

Origin of Bentonites and Detrital Zircons of the Paleocene Basilika Formation, Svalbard

Felix J. Elling1,2*, Cornelia Spiegel1*, Solveig Estrada3, Donald W. Davis4, Lutz Reinhardt3, Friedhelm Henjes-Kunst3, Niklas Allroggen1, Reiner Dohrmann3, Karsten Piepjohn3 and Frank Lisker1
  • 1Department of Geosciences, University of Bremen, Bremen, Germany
  • 2MARUM – Center for Marine Environmental Sciences, University of Bremen, Bremen, Germany
  • 3Federal Institute for Geosciences and Natural Resources (BGR), Hannover, Germany
  • 4Department of Geology, University of Toronto, Toronto, ON, Canada

The Paleocene was a time of transition for the Arctic, with magmatic activity of the High Arctic Large Igneous Province (HALIP) giving way to magmatism of the North Atlantic Large Igneous Province in connection to plate tectonic changes in the Arctic and North Atlantic. In this study we investigate the Paleocene magmatic record and sediment pathways of the Basilika Formation exposed in the Central Tertiary Basin of Svalbard. By means of geochemistry, Sm–Nd isotopic signatures, and zircon U–Pb geochronology we investigate the characteristics of several bentonite layers contained in the Basilika Formation, as well as the provenance of the intercalated clastic sediments. Our data show that the volcanic ash layers of the Basilika Formation, which were diagenetically altered to bentonites, originate from alkaline continental-rift magmatism such as the last, explosive stages of the HALIP in North Greenland and the Canadian Arctic. The volcanic ash layers were deposited on Svalbard in a flat shelf environment with dominant sediment supply from the east. Dating of detrital zircons suggests that the detritus was derived from Siberian sources, primarily from the Verkhoyansk Fold-and-Thrust Belt, which would require transport over ~3000 km across the Arctic.

Introduction

The Paleogene was a time of profound change in the Arctic realm (Figure 1): caused by the contemporaneous spreading in the Baffin Bay/Labrador Sea and the North Atlantic, Greenland moved north and collided with Svalbard in the East and with Ellesmere Island (Canadian High Arctic) in the West (e.g., Talwani and Eldholm, 1977; Roest and Srivastava, 1989; Tessensohn and Piepjohn, 2000; Oakey and Chalmers, 2012). This led to the so-called Eurekan deformation that affected North Greenland, Ellesmere Island and Svalbard, and caused the formation of the West Spitsbergen Fold-and-Thrust Belt on Svalbard (e.g., Tessensohn and Piepjohn, 2000). Detailed timing of Eurekan deformation is still poorly constrained, but presumably commenced in the Paleocene, culminated in the Eocene, and may have lasted into the Oligocene (Tessensohn and Piepjohn, 2000; Piepjohn et al., 2013). Concurrent with Eurekan compression, extension prevailed further north, leading to the onset of spreading along the Gakkel Ridge, separation of the Lomonosov Ridge from the Barents Sea Shelf and the opening of the Eurasia Basin (e.g., Pitman and Talwani, 1972; Srivastava, 1985; Jackson and Gunnarsson, 1990; Tessensohn and Piepjohn, 2000; Døssing et al., 2013b). While the convergent movements were seemingly not associated with magmatic activity (cf. Tessensohn and Piepjohn, 2000), extensional tectonics were accompanied by magmatism with continental rift signature from the Early Cretaceous onwards until ~61 Ma (e.g., Tarduno, 1998; Estrada et al., 2001; Maher, 2001; Tegner et al., 2011; Thorarinsson et al., 2011b). During the Paleogene, magmatism in the Arctic was predominantly intrusive and basaltic effusive (e.g., Storey et al., 1998; Tegner et al., 1998; Storey et al., 2007; Thorarinsson et al., 2011b), but explosive volcanic activity also occurred, as evidenced by volcanic ash layers on Ellesmere Island and Svalbard (e.g., Dypvik and Nagy, 1978; Reinhardt et al., 2013). These ash layers are preserved in Paleogene sediments, i.e., in the Eureka Sound Group on Ellesmere Island and in the Central Tertiary Basin on Svalbard (Dypvik and Nagy, 1978; Reinhardt et al., 2013). Both depocenters are dominated by clastic deposition, and their stratigraphy and provenance are still poorly resolved (e.g., Miall, 1991; Dallmann, 1999). For the Central Tertiary Basin, a sediment source from the rising West Spitsbergen Fold-and-Thrust Belt to the west is assumed from ~mid-Eocene onwards (e.g., Helland-Hansen, 1990). Before that time, during the Paleocene and early Eocene, the basin received detritus from easterly directions, where a not further specified highland must have undergone active erosion (e.g., Helland-Hansen, 1990; Bruhn and Steel, 2003).

FIGURE 1
www.frontiersin.org

Figure 1. Overview over the tectono-magmatic framework of the Arctic and North Atlantic oceans indicating two major magmatic phases expressed in the late Cretaceous high arctic large igneous province (HALIP) and the Paleocene-Eocene North Atlantic volcanic province (NALIP) as well as the widespread occurrence of Paleocene to Eocene ash deposits (compiled from Knox and Morton, 1988; Hopper et al., 2003; Larsen et al., 2003a; Storey et al., 2007; Estrada et al., 2010; Tegner et al., 2011; Reinhardt et al., 2013, and references therein).

This study focuses on the Paleocene Basilika Formation of the Central Tertiary Basin on Svalbard. This formation comprises deltaic to deep-water clastic sediments (e.g., Steel et al., 1981), supposedly sourced from the east (Steel et al., 1981; Helland-Hansen, 1990; Müller and Spielhagen, 1990), and contains several altered volcanic ash layers that were previously characterized as bentonites (e.g., Gripp, 1927; Nagy, 1966; Dypvik and Nagy, 1978). The primary aim of this study is to geochemically characterize the Basilika bentonites in order to derive information on the origin of their volcanic sources and their plate tectonic environment. Furthermore, the ash layers will be compared to the Paleocene bentonites occurring on Ellesmere Island, to test whether both volcanic deposits may have derived from the same source (taking into account that Ellesmere Island and Svalbard were situated relatively close to each other during the Paleocene). For this, we performed main and trace element geochemical as well as Sm-Nd isotope analyses on the Basilika Formation bentonites as well as on the Ellesmere Island bentonites (complementing the data published by Reinhardt et al., 2013). No primary magmatic zircons were found in the bentonites, but we used U–Pb dating of detrital zircons contained in the bentonites to characterize the provenance of the Basilika Formation and to constrain the paleogeographic setting and sediment transport pathways during the Paleocene.

Geological Setting

Cretaceous-Paleogene Geology of Svalbard and Regional Tectono-Magmatic Framework

The Svalbard archipelago represents the uplifted north-western margin of the Barents shelf and is confined to the north by the Eurasia Basin of the Arctic Ocean and to the west by the Fram Strait (Figure 1). Svalbard has a complex tectono-magmatic history comprising multiple orogenies and magmatic events, which is to a great extent shared with that of the circum-arctic land masses, most prominently by Ellesmere Island and Greenland, but also with Baltica.

During the Cretaceous the northernmost regions of Ellesmere Island, Greenland and Svalbard were adjacent to each other at a paleolatitude of about 80°N (Lawver et al., 1990; Faleide et al., 1993; Harland, 1997). During the Early Cretaceous, fine-clastic sediments were deposited on Svalbard, followed by delta progradation from the northwest to the southeast with sediment transport possibly from Greenland (Røhr, 2009). Exhumation and erosion of northern Svalbard caused by the opening of the Amerasia Basin during the Cretaceous may have provided another source of detritus feeding the prograding delta system (Dörr et al., 2013). The Early Cretaceous sediments of Svalbard are truncated by an erosional unconformity and hence Late Cretaceous strata are completely missing (Dallmann, 1999).

Intrusive and extrusive magmatism on Svalbard in the Early Cretaceous was coeval with widespread volcanism throughout the Arctic and connected to the formation of the Cretaceous (to Paleogene) High Arctic Large Igneous Province (HALIP) (Tarduno, 1998; Maher, 2001). The HALIP is manifested in Cretaceous flood basalts, dykes and sills on eastern Svalbard and the adjacent subseafloor (Maher, 2001; Minakov et al., 2012; Corfu et al., 2013), Franz Josef Land, Ellesmere Island, and other islands in the Canadian Arctic (Embry and Osadetz, 1988; Estrada and Henjes-Kunst, 2004, 2013; Corfu et al., 2013; Jowitt et al., 2014), as well as Late Cretaceous to Paleocene dykes and extrusive magmatism on northern Greenland and the Canadian Arctic islands (Figure 1; e.g., Estrada et al., 2001; Kontak et al., 2001; Tegner et al., 2011; Thorarinsson et al., 2011a).

The HALIP comprises a tholeiitic suite (ca. 130–90 Ma) and an alkaline suite (ca. 90–60 Ma; Estrada and Henjes-Kunst, 2004; Buchan and Ernst, 2006; Tegner et al., 2011; Thorarinsson et al., 2011b; Estrada, 2015). The tholeiitic suite is associated with extensional tectonics in the High Arctic related to the breakup of the Arctic continental land masses and the subsequent opening of the Amerasia Basin (Tegner et al., 2011; Døssing et al., 2013b). The extrusion of the alkaline suite of the HALIP is typical for continental rifts and does only partly overlap geographically with the tholeiitic suite (Tegner et al., 2011). Alkaline mafic to felsic volcanism is known from northwest Ellesmere Island (Hansen Point Volcanic Complex at around 80 Ma; Embry and Osadetz, 1988; Estrada and Henjes-Kunst, 2004, 2013), the Kap Washington Group in North Greenland (71–61 Ma; Tegner et al., 2011; Thorarinsson et al., 2011a,b), from the Cape Back Basin on Ellesmere Island, evidenced by deposition of volcanogenic detritus (61–58 Ma; Estrada et al., 2010) and from Freeman Cove, Bathurst Island (56 Ma; Day et al., 2005; Figure 1).

In the High Arctic volcanism ceased during the Paleogene probably due to compressional tectonics induced by the northwards movement of Greenland (Tegner et al., 2011). Coevally with the termination of volcanism in the High Arctic, a Large Igneous Province formed in the North Atlantic region (NALIP). The NALIP is expressed in flood basalts on eastern Greenlandas well as flood basalts and alkaline tuffs in western central Greenland (Storey et al., 1998, 2007; Tegner et al., 1998; Larsen and Pedersen, 2009; Larsen et al., 2016). Moreover, Paleocene bentonites were observed on Svalbard as well as Ellesmere Island and are particularly widespread in the North Atlantic region (Figure 1; Major and Nagy, 1972; Dypvik and Nagy, 1978; Larsen et al., 2003a; Grist and Zentilli, 2004; Reinhardt et al., 2013).

Until ~55 Ma, Greenland was part of the Eurasian plate. The plate boundaries between the Eurasian and North American plates were located in the Labrador Sea/Baffin Bay and within the Eurasia Basin. Both plate boundaries were connected by a putative sinistral transform fault, the existence and exact positioning of this fault currently being under debate (e.g., Tessensohn and Piepjohn, 2000; Oakey and Chalmers, 2012; Greiner and Neugebauer, 2013; Frisch and Dawes, 2014; Neugebauer and Greiner, 2014). From 55 Ma onwards, Greenland was separated from both Eurasia and North America by coeval seafloor spreading in the Labrador Sea/Baffin Bay and in the northern North Atlantic Ocean (Pitman and Talwani, 1972; Roest and Srivastava, 1989; Tessensohn and Piepjohn, 2000), as well as in the Eurasia Basin (Tessensohn and Piepjohn, 2000). Seafloor spreading in the Labrador Sea/Baffin Bay ceased at ~33 Ma (Kristoffersen and Talwani, 1977), while the North Atlantic spreading system continued to propagate northwards, separating Greenland/North America from Eurasia/Svalbard from the Oligocene onwards (e.g., Talwani and Eldholm, 1977; Gaina et al., 2009, 2015; Seton et al., 2012; Døssing et al., 2013a, 2016).

The northwards movement of Greenland as an independent micro-plate between 56 and 33 Ma led to intracontinental compression along the margins of Eurasia and North America, which is expressed in the Eurekan deformation of Svalbard, northeast Greenland, and Ellesmere Island (Tessensohn and Piepjohn, 2000; CASE Team, 2001). These deformations were initiated during the Early Paleocene and culminated during the Eocene (Oakey and Chalmers, 2012; e.g., Piepjohn et al., 2013), forming the West Spitsbergen Fold-and-Thrust Belt (Bergh et al., 1997; Piepjohn et al., 2001; von Gosen and Piepjohn, 2001). The NNW-SSE striking Central Tertiary Basin (CTB, Figure 2) was formed as a foreland basin of the fold-and-thrust belt and filled with the eroded material of the bulge. Compression in the West Spitsbergen Fold-and-Thrust Belt ceased during the Late Eocene followed by a short extensional episode during the early Oligocene (Braathen et al., 1999; CASE Team, 2001).

FIGURE 2
www.frontiersin.org

Figure 2. Geological map of Svalbard showing the location of the working area in 2010 (open rectangle; Figure 3) within the Central Tertiary Basin of Spitsbergen (CTB; based on Dallmann, 1999). Diamonds indicate sampling sites during the CASE 1 expedition in 1992.

Stratigraphy of the Central Tertiary Basin (CTB)

The main occurrence of Paleogene strata on Svalbard is in the CTB of Spitsbergen (Figure 2), the main island of the Svalbard archipelago (reviewed in Dallmann, 1999). The CTB comprises a Paleocene to Eocene clastic sedimentary sequence, the Van Mijenfjorden Group, with a preserved thickness of more than 1900 m, which lies unconformably upon Lower Cretaceous sandstones of the Carolinefjellet Formation (Figures 3A, 4; Major and Nagy, 1964; Livšic, 1967; Harland, 1969; Major and Nagy, 1972; Livšic, 1974; Dallmann, 1999).

FIGURE 3
www.frontiersin.org

Figure 3. (A) Stratigraphic position of the Basilika Formation within the Van Mijenfjorden Group in the Bjørndalen area (viewed from NW). (B) Geologic map of Bjørndalen (based on Major et al., 2001) showing sampling locations.

FIGURE 4
www.frontiersin.org

Figure 4. Paleogene stratigraphy of the Central Tertiary Basin of Spitsbergen (modified from Steel et al., 1985; Uroza and Steel, 2008; Charles et al., 2011).

The base of the Van Mijenfjorden Group is formed by the Paleocene Firkanten and Basilika formations. These represent an overall transgressive succession, evolving from continental to marginal marine sandstones of the Firkanten Formation to the marine shales of the Basilika Formation (Steel et al., 1981; Figure 4). The Basilika Formation consists of black mudstones, shales and siltstones with intercalated bentonite horizons that were deposited in a prodelta environment (Steel et al., 1985; Müller and Spielhagen, 1990). The lower part of the formation features a fining upwards sequence, which reverses into coarsening upwards in the upper part of the formation (Dallmann, 1999). This upper part of the formation marks the onset of a regression, leading to a gradual transition from marine shales into the marine glauconitic, highly bioturbated sandstones of the Grumantbyen Formation (Steel et al., 1981). The overlying strata comprise a transgression-regression cycle recorded in the Paleocene-Eocene Frysjaodden Formation and the Eocene Battfjellet and Aspelintoppen formations (Charles et al., 2011; Figure 4). Sedimentation in the CTB ceased during the Middle Oligocene (Harland, 1997). The thickness of the Paleogene formations varies greatly throughout the CTB. The Basilika Formation thins out from more than 350 m in the southwest to ~10 m in the northeast (Dallmann, 1999).

Bentonites are very common in the Basilika Formation. They were first described by Gripp (1927) as thin, laterally consistent beds of plastic clay and have been observed in several locations within the CTB (Nagy, 1966; Vonderbank, 1970; Major and Nagy, 1972; Dypvik and Nagy, 1978; Major et al., 2001). Dypvik and Nagy (1978) described the bentonites as very fine-grained but poorly sorted, with maximum grain sizes between 15 and 40 μm and consisting of ~80% clay minerals—mostly illite/smectite—with minor fractions of quartz and feldspar, indicative of altered, aeolian-transported volcanic material. Based on the grain size they concluded that the source area was located at a distance of 100−200 km from the area of deposition but more distant sources were not excluded. Except for the bentonites of the Basilika Formation, only few indications of Paleogene volcanism have been found on Svalbard. Major and Nagy (1972) reported that bentonites of 10−20 cm thickness had been observed adjacent to the coal seams of the Firkanten Formation. Further bentonite layers of Paleocene age are known from numerous coal exploration wells (Jones et al., 2015). Additionally, bentonites were observed in the Frysjaodden Formation, situated in the interval of the carbon isotope excursion of the Paleocene-Eocene Thermal Maximum, and thus provide constraints on the numerical age of the Paleocene-Eocene boundary on Spitsbergen (Charles et al., 2011).

The biostratigraphy of the Van Mijenfjorden Group is poorly resolved (reviewed in Manum and Throndsen, 1986; Čepek and Krutzsch, 2001). While earlier publications proposed just a Paleocene age for the Firkanten Formation (Manum, 1962), more recent studies place it in the Selandian to Thanetian (Middle to Upper Paleocene) based on the occurrence of a coccolithophore species (Čepek, 2001; Čepek and Krutzsch, 2001). Normapolles flora found in the Basilika Formation was assigned to a wide age range from uppermost Cretaceous to middle Paleocene (Čepek and Krutzsch, 2001). Manum and Throndsen (1986) suggested that the Basilika Formation was deposited in the Lower to Upper Paleocene transition based on dynocysts. However, a Danian (Early Paleocene) age for the lower part of the Basilika Formation is not very likely due to the Middle to Upper Paleocene deposition age of the underlying Firkanten Formation (Čepek, 2001; Čepek and Krutzsch, 2001). The Late Paleocene age of the overlying Grumantbyen Formation is again poorly constrained. The Grumantbyen Formation is overlain by the Frysjaodden Formation, which contains a bentonite layer dated as 55.9 ± 0.1 Ma (Paleocene/Eocene boundary after Gradstein et al., 2012) by U–Pb geochronology (Charles et al., 2011). Summarizing the biostratigraphic and radiometric age constraints as well as the lithostratigraphic correlations for the CTB formations and considering recent changes in the Geologic Time Scale, a latest Danian to early Thanetian time interval (ca. 62–58 Ma) for the deposition of the Basilika Formation can be estimated.

Sampling and Field Observations

The Bjørndalen section of the Basilika Formation consists of two outcrops along the river Bjørndalselva and contains a total of four bentonite layers (Table 1, Figures 3, 5). The sandstone cliffs of the Firkanten Formation are well above the river at the seaward valley entrance (Figure 3A). Further up the valley, the river cuts first into the Firkanten Formation and subsequently into the Basilika and Grumantbyen Formations, forming well exposed outcrops. The exposures of the Firkanten and Basilika Formations along the river were logged stratigraphically (Figure 5).

TABLE 1
www.frontiersin.org

Table 1. Bentonite sampling sites on Svalbard (sample labels denote replicate samples from adjacent locations of the same horizon).

FIGURE 5
www.frontiersin.org

Figure 5. Stratigraphic log (A) and sampled outcrops (B–F, insets are not to scale) of the Basilika Formation at Bjørndalselva, inner Bjørndalen. Bentonite thicknesses are exaggerated for visibility. Sandstone grain size indicated as vf, very fine; f, fine; m, medium; c, coarse; vc, very coarse.

The lower, middle, and uppermost parts of the Firkanten Formation are scree-covered, so that just a section of 11.5 m of the upper part could be investigated. The formation comprises mostly fine-grained sandstones with intercalated siltstones and silty shales with an overall fining upwards trend. Mudclasts, clay-ironstone nodules as well as coal or plant fragments are frequent in the upper part. Bioturbation is common throughout the investigated section. The Basilika Formation is 73.5 m thick, dips 5°SE and is partly debris-covered. Therefore, the boundary to the underlying Firkanten Formation could not be observed and the outcrop of the Basilika Formation is split into several parts. The Basilika Formation consists of dark gray to black, silty shales, and siltstones with few intercalated sandstone horizons. Bioturbation is common in the lower part of the formation but absent in the middle and upper part. The formation comprises several coarsening upwards sequences from shale to siltstone. Dropstones, mostly in the range of 1–5 cm in diameter but rarely up to 20 cm can be observed throughout the formation. These consisted in all cases either of chert or quartz/quartzite. The boundary between the Basilika Formation and the overlying Grumantbyen Formation is well exposed and marked by the occurrence of a fine-grained glauconitic sandstone bed.

Two pairs of laterally continuous horizons of plastic, gray-weathered brownish clay were observed in the Basilika Formation and interpreted as bentonites. Horizons H1 and H2 are located in the lower part of the formation about 50 cm apart and are 5 and 3 cm thick, respectively. Horizons H3 and H4 are located in the middle part of the formation and are 2 m apart, with thicknesses of 3 and 5 cm, respectively. Horizon H3 was subdivided into a main horizon and sub-horizon H3b. The latter does not form a coherent layer but occurs sporadically several cm above the H3 main horizon.

The bentonite layers comprise plastic, gray-weathered brownish clay intercalated into shales of the lower Basilika Formation (Horizons H1 and H2) and siltstones of the upper Basilika Formation (H3 and H4; Table 1, Figure 5). The horizons were laterally traceable as continuous lines of vegetation on the scree cover. Two to three samples were taken from each horizon (about 1.5 kg per horizon) in 2010 for petrographic, geochemical, and geochronological analyses (see Table 1 for sample numbers).

For geochemical comparisons, additional bentonite samples from the Basilika Formation collected during the CASE 1 expedition of the German Federal Institute for Geosciences and Natural Resources (BGR) in 1992 (Tessensohn et al., 2001) and two bentonite samples from the lower Paleogene Mount Lawson Formation (Eureka Sound Group) of Ellesmere Island, Canada (Reinhardt et al., 2013) were included in this study. Whole-rock geochemical data of bentonites of the Basilika Formation sampled during the CASE 1 expedition in 1992 in the northern part of the CTB complements the dataset obtained in this study (Supplementary Material). The sampling sites of the CASE 1 bentonites are located on the Erdmannflya peninsula on the northern shore of Isfjorden, as well as in Fossildalen, Russekollen, and Battfjellet to the southwest of Longyearbyen (Table 1, Figure 2). Their stratigraphic positions relative to the bentonites recovered in Bjørndalen is unknown.

Analytical Methods

Compositional Analyses

Sample preparation and compositional analyses were conducted at the Federal Institute for Geosciences and Natural Resources (BGR) in Hannover, Germany. Identification of mineral phases and geochemical analyses were initially performed on homogenized whole-rock samples. Subsequently, clay fractions (<2 μm) were separated from the whole-rock samples using ultrasonication and analyzed separately in order to minimize the influence of detrital components. Identification of mineral phases in whole-rock samples and <2 μm fractions was achieved by infrared spectroscopy and X-ray diffraction (XRD; Cu radiation) measurements of air dried and ethylene glycol vapor-solvated samples. Cation-exchange capacity (CEC) was measured as a qualitative indicator for bentonite using Cu-trien (Dohrmann et al., 2012). Additionally, scanning electron microscopy was performed on samples H2 and H3 for identification of volcanic glass particles. The chemical composition of the whole-rock samples and <2 μm fractions was analyzed by X-ray fluorescence (XRF) spectrometry and inductively-coupled plasma mass spectrometry (ICP-MS). Sm–Nd isotope data were obtained on the acid-digested whole-rock samples and <2 μm fractions. U-Pb ages of density-separated, hand-picked zircons were determined using laser ablation ICP-MS (LA-ICP-MS). Concordia diagrams were plotted using the Isoplot program of Ludwig (1991). Probability density plots were created using a program written by Sircombe (2004). 206Pb/238U ages are plotted for zircons < 1000 Ma and 207Pb/206Pb ages for zircons >1000 Ma. A detailed description of the methods can be found in the Supplementary Material (Section Analytical Methods). Results are given in Tables 2, 3 and the Supplementary Material. All data are stored in the Pangaea database and are accessible via http://doi.pangaea.de/10.1594/PANGAEA.860807.

TABLE 2
www.frontiersin.org

Table 2. Chemical composition of Basilika Formation (Bjørndalen area) and Mount Lawson Formation bentonites (<2 μm fractions) determined by X-ray fluorescence and ICP-MS.

TABLE 3
www.frontiersin.org

Table 3. Sm-Nd isotope data of bentonite samples (<2 μm fractions) from Svalbard and Ellesmere Island.

Results and Interpretation

Mineralogical Composition of the Basilika Formation Bentonites

Multiple lines of evidence indicate that the plastic clay horizons in the Basilika Formation are indeed bentonites. XRD analyses on the whole-rock powder samples revealed a composition dominated by quartz, feldspar, and smectite-rich interstratified (mixed-layered) minerals for all samples. While all samples contain traces of kaolinite and muscovite-illite, only the lower horizons H1 and H2 additionally comprise traces of anatase (TiO2) and barite (observed during heavy mineral separation). High loss on ignition (6.5–10.0 wt%; see Supplementary Material) in all samples and a lack of relict volcanic glass indicate strong alteration of the primary volcanic ashes. The <2 μm fractions were analyzed separately to obtain a more comprehensive characterization of the clay minerals. The clay fractions showed CEC values of 27–35 meq/100 g (H1 and H2) and 24–32 meq/100 g (H3 and H4), consistent with a high abundance of clay minerals, but lower than the CECs typical for smectite-rich bentonites (Rollins and Pool, 1968; Reinhardt et al., 2013). XRD analysis of air-dried and ethylene glycol solvated samples revealed that the <2 μm fractions were dominated by illite-smectite type expandable clay minerals, with R0 illite (0.45)-smectite in samples H1 and H2 and R1 illite (0.6)-smectite in samples H3 and H4 (Figure 6). This is consistent with previous observations (Dypvik and Nagy, 1978). Furthermore, quartz, kaolinite, and chlorite (Figure 6) were present in all <2 μm fractions, while anatase was abundant in samples H1 and H2 (Figure 6). The dominance of illite-smectite in contrast to smectite in other bentonites might be indicative of diagenetic transformation of smectite to illite (Šucha et al., 1993), consistent with the burial history of the CTB (Blythe and Kleinspehn, 1998) and is therefore a further indication of the strong diagenetic alteration of the bentonites.

FIGURE 6
www.frontiersin.org

Figure 6. (A) X-ray powder diffraction (XRD) patterns of samples (fraction < 2 μm) from four bentonite horizons of the Basilika Formation. (B,C) Comparison of XRD patterns of air dried and ethylene glycol solvated bentonite samples (<2 μm) from horizons H2 and H4 containing R0 illite(0.45)-smectite (B) and R1 illite(0.60)-smectite (C).

Geochemical and Isotopic Characterization of the Basilika Formation Bentonites

To largely exclude detrital contaminants, major and trace element geochemical analyses and Sm-Nd isotope ratio measurements were performed using the <2 μm fraction assuming that the clay minerals represent the alteration products of the original volcanic glass.

The bentonite samples exhibited similar SiO2 concentrations (45–47 wt%; Table 2). They can be divided into two groups, a stratigraphically older suite comprising H1 and H2 with elevated TiO2 (~5 wt%) and lower Al2O3 (~20 wt%) abundances and a younger group comprising H3 to H4 with lower TiO2 (~1 wt%) and higher Al2O3 (~23 wt%) contents. Furthermore, the K2O content is slightly higher in H3 and H4 (~3.5 wt%) compared to H1 and H2 (~2.5 wt%). Additionally, V, Cu, and Sc are higher in H1 and H2, whereas Nb, Y, Th, Zr, and the rare earth elements (REE; except Eu) are higher in H3 and H4 (Supplementary Material).

The geochemical fingerprint of the analyzed bentonites was in part inherited by the parental volcanic ashes but likely also influenced by post-depositional alteration. Alteration may have occurred at several stages. Firstly, alteration by seawater via ion exchange after deposition of the ashes in the pelagic zone of the marine basin, which occupied the CTB during the time of deposition. Subsequently, the volcanic glass and the less stable minerals were transformed to clay and other minerals. Finally, the volcanic ashes may have been altered by diagenesis at a burial depth of up to 2 km, which was followed by Neogene uplift and exhumation as well as recent weathering (Blythe and Kleinspehn, 1998; Dörr et al., 2013; Schlegel et al., 2013). During all of these phases, ions may have been exchanged with the surrounding rocks and water, thus altering the original geochemical fingerprint. Specifically, seawater-mediated alteration of felsic and intermediate volcanic rocks to bentonites may result in leaching of Na, K, Sr, Rb, as well as uptake of Mg and Fe2+, while Al, Ti, Zr, Nb, V, and Ni are residually enriched and the behavior of Si and Ca depends on the chemistry of the parent rock (Christidis, 1998). Similarly, seafloor alteration of basaltic ashes may result in enrichment in Si and Al as well as depletion in Fe, Mg, and Ca (Larsen et al., 2003a). Furthermore, the diagenetic transformation of smectite to illite should theoretically yield enrichment in K and Al and decrease in Mg and Na content, based on the stoichiometry of the montmorillonite and illite end members. Therefore, conventional discrimination diagrams for the characterization of the volcanic source rocks may not be applicable to the classification of bentonites. Still, the strong systematic differences in TiO2 and Al2O3 content among the Basilika Formation bentonites likely originate from differences in the chemical composition of the volcanic ash precursors and may therefore be characteristic for the magmatic source.

The behavior of the REE and Y during alteration is controlled by the presence of phosphate minerals (Christidis, 1998; Reinhardt et al., 2013). There is no indication for the presence of such minerals in the Basilika bentonite samples. Furthermore, the concentrations of REE and Y are generally higher in the <2 μm fraction than in the whole-rock fraction (see Supplementary Material) indicating that these elements are hosted by the clay minerals (as most other trace elements, except Ba and Sr). Thus, we infer that the REE and some other relatively immobile trace elements (e.g., Zr, Ti, Y, Nb) as well as their ratios can provide a geochemical fingerprint of the parent volcanic ash. The chondrite-normalized REE patterns of the bentonite samples generally show enrichment of light REE (LREE) vs. heavy REE (HREE) with H1 and H2 (Lan/Lun = 11−12) being less enriched than H3 and H4 (Lan/Lun = 15−19) (Figure 7). In the range of the HREE, the patterns are subparallel to each other (Tbn/Lun = 1.9−2.2 for H1/H2 and 2.1−2.3 for H3/H4), indicating magma generation under similar conditions with the H3/H4 magma being more evolved compared to H1/H2. This is supported by a negative Eu anomaly increasing from H1 (Eu/Eu* = 0.87) to H4 (Eu/Eu* = 0.59) indicating fractional crystallization of feldspar (Philpotts and Schnetzler, 1968). An alkali-basaltic original ash composition is suggested for the H1 and H2 bentonites, while a trachytic to alkali-rhyolitic original ash composition is suggested for the H3, H3b, and H4 bentonites, assuming that the Zr/Ti and Nb/Y ratios are only slightly affected by alteration processes (Figure 8). Thus, the younger bentonites on Svalbard (H3–H4) originated from a more evolved magma than the older bentonites (H1–H2).

FIGURE 7
www.frontiersin.org

Figure 7. Chondrite normalized rare earth element (REE) patterns (A) of bentonite horizons of the Bjørndalen section (<2 μm fraction) and (B) of bentonites from other outcrops of the Basilika Formation sampled during the CASE 1 expedition (whole rock), and (C) REE patterns of two Paleogene bentonites from the Mount Lawson Formation (Ellesmere Island, <2 μm fraction), alkaline volcanic detritus from the Cape Back Basin, Nares Strait (Estrada et al., 2010), and an alkaline flood basalt from Disko Island (Larsen et al., 2003b) for comparison. REE patterns of the Bjørndalen section bentonites are shaded gray in (B,C). Chondrite data from Sun and McDonough (1989).

FIGURE 8
www.frontiersin.org

Figure 8. Zr/Ti-Nb/Y discrimination diagram (after Winchester and Floyd, 1977; Pearce, 1996) of Basilika Formation bentonites as well as two Paleogene bentonites from the Mount Lawson Formation (Ellesmere Island; whole-rock data from Reinhardt et al., 2013), alkaline volcanic detritus from the Cape Back Basin, Nares Strait (Ellesmere Island; Estrada et al., 2010) and an alkaline flood basalt from Disko Island (Greenland; Larsen et al., 2003b) for comparison. Black symbols, <2 μm fraction; Gray symbols, whole rock.

The high Zr concentrations of up to ~2400 ppm in the <2 μm fractions potentially represent a combination of inheritance from the precursor rock and detrital contamination. Since no major Zr-bearing mineral phase could be identified, the Zr was likely associated with the glass matrix of the precursor rock resulting from rapid cooling before any zircon could crystallize. Likewise, high Zr concentrations have been observed in melt inclusions in Paleogene alkaline tuffs from Greenland (Heister et al., 2001). In contrast, contamination by detrital zircons during deposition or diagenesis could also lead to elevated Zr concentrations of the bentonites. However, the interlayered sandstones of the Basilika Formation have up to tenfold lower Zr concentrations (Schlegel et al., 2013), which are well within the range commonly observed for sedimentary rocks and upper continental crust (Taylor and McLennan, 1985). A detrital origin of the high Zr concentrations in the <2 μm fractions would thus require extraordinarily strong, selective enrichment of zircon in this size class, which is not commonly observed during diagenesis of sedimentary and magmatic rocks (González López et al., 2005; Taboada et al., 2006; Cavalcante et al., 2014). Contrasting evidence for contamination by detrital zircons comes from the distinct Zr/Nb ratios of the bentonites. The high Nb contents of H1-H4 (75–142) suggest that the bentonites originate from alkaline precursor rocks. Indeed, the Zr/Nb ratios of around 7 for H1 and H2 are well within the range suggested for alkaline rocks (<10; Larsen et al., 2003a), while those of H3 and H4 (~12−21) are far higher. Assuming that Zr and Nb are mobile to a similar degree during diagenesis, this would suggest that contamination by detrital zircons is negligible for H1 and H2, while up to half or more of the Zr content in H3 and H4 could be derived from detrital material. Accounting for this detrital Zr would yield lower Zr/TiO2 ratios for H3/H4 and would thus suggest a lower degree of magmatic differentiation. However, the Zr/TiO2 vs. Nb/Y discrimination diagram would still indicate that H3/H4 originate from a more evolved magma than H1/H2 even when accounting for a large degree of contamination by detrital Zr of 50% or more.

The different enrichment of LREE vs. HREE in H1/H2 and H3/H4 likely reflects different degrees of partial melting of the mantle source. A similar mantle source is supported by the Sm–Nd isotope data (Table 3). The εNd(t) values of H1/H2 (1.2–1.3) and H3/H4 (0.3–1.6) overlap and the Nd model ages (tDM) vary in a narrow range for all horizons (0.55–0.67 Ga). This mantle source is very similar to those of alkaline basalts from ocean island and continental rifting settings (Wilson, 1989), pointing to either a fertile mantle source as in hot-spot settings, melting in the subcontinental lithospheric mantle and/or the contamination of the magma by continental crust. Overall, the REE data of the H1–H4 bentonites suggest that all analyzed ash layers were sourced from the same tectono-magmatic setting and possibly also from the same volcanic center within a continental rift zone, exhibiting minor differences in the parental magma composition and different degrees of differentiation.

Based on the Zr/Ti-Nb/Y discrimination diagram, the CASE 1 bentonites originate from an alkaline magmatic suite (Figure 8). Their whole-rock REE can be subdivided into two groups: A group with highly enriched LREE vs. HREE and a group with less enriched LREE vs. HREE and a trough in the HREE from Tb to Lu that is probably the result of stronger alteration (Figure 7B). The REE patterns of the second group actually look similar to pelitic sediments, but the positive εNd(t) value of sample TH 145 and the small positive Eu anomalies of the FTS 78 samples point to a volcanic origin. The small positive Eu anomalies point to a source in North Greenland or northeastern Ellesmere Island (Thorarinsson et al., 2011a; Estrada, 2015). The REE patterns of the FTS 35−36 samples (Erdmannflya) are similar to those of the geochemically evolved Bjørndalen bentonites H1 and H4, but are steeper. The REE pattern of sample TH 144 is comparable to those of H3 and H4, but the Sm-Nd data of this sample [εNd(t) = −0.9; tDM = 0.9 Ga] indicate stronger contamination with crustal materials or potentially a different mantle source. Thus, the bentonite layers sampled during CASE 1 cannot be considered to be equivalents of the Bjørndalen bentonites, although they originate most likely also from continental-rift related magmatism. The geochemical fingerprints of the CASE 1 samples indicate that different volcanic centers may have sourced the various bentonite layers within the Basilika Formation.

Results of Zircon U–Pb Dating

All four samples from the Basilika Formation yielded similar zircon populations consisting mostly of subrounded and rounded zircon that varied from colorless to pale violet. Euhedral grains were rare and tended to be small. U–Pb LA-ICP-MS analyses were performed on a total of 430 zircons from the four bentonite horizons (Supplementary Material). The 261 zircon age analyses with ≤10% central discordance were used for further interpretation (Figure 9). Age distributions were highly similar between the four samples from the Basilika Formation, indicating constant sediment sources during deposition (Figure 10). The zircon ages with < 10% discordance span a range from 88 ± 1 Ma to 2950 ± 10 Ma (Supplementary Material) that can be subdivided into four distinct populations (Figure 10):

(i) Neoarchean (2500–2800 Ma) with a peak at 2700–2800 Ma;

(ii) Paleoproterozoic (1700–2100 Ma) with a peak around 1800−1900 Ma;

(iii) a small population at ca. 900–1000 Ma (8 of 11 ages between 974 Ma and 995 Ma);

(iv) a broad cluster of ages scattered fairly uniformly between 200 and 650 Ma.

FIGURE 9
www.frontiersin.org

Figure 9. Concordia diagrams of LA-ICP-MS U-Pb analyses of zircons from four bentonite horizons (H1-H4, panels A–D) of the Basilika Fm. Error ellipses represent 95% confidence limits.

FIGURE 10
www.frontiersin.org

Figure 10. Frequency (gray) and relative probability (blue) plots of zircon U-Pb ages with ≤10% central discordance (A, all ages; B, 0–1000 Ma) from four bentonite horizons of the Basilika Fm. 206Pb/238U ages are plotted for zircons <1000 Ma and 207Pb/206Pb ages for zircons >1000 Ma.

Only a few scattered ages <200 Ma are present (88 ± 1, 152 ± 1, 154 ± 2, 162 ± 1, 188 ± 3 Ma), all older than the Paleocene depositional age of the Basilika Formation. The pale violet grains are mostly Precambrian in age. The euhedral grains show a similarly wide age range as the subrounded ones, although the youngest grains are mostly euhedral. Thus, morphology cannot be used as a discriminant for primary volcanic zircons. Th/U profiles for many of the younger grains show a characteristic, step change from low to high ratios that might indicate the presence of core-overgrowth relationships. Therefore, LA-ICP-MS profiles were measured over a single component where possible, but in some cases ages may represent mixtures of Neoproterozic and Phanerozoic components.

Only 18 concordant zircon ages were detected in the Ellesmere Island samples, which cluster around 1800−2000, 2500−2900 Ma, with minor age groups around 1500−1700 and 1000−1200 Ma (Figure 11). Mesozoic/Paleozoic ages are almost completely absent.

FIGURE 11
www.frontiersin.org

Figure 11. Frequency (gray) and relative probability (blue) plots of zircon U-Pb ages with ≤10% central discordance from two bentonite horizons (Lawson ash 1 and 2) of the Mount Lawson Formation, Ellesmere Island. 206Pb/238U ages are plotted for zircons <1000 Ma and 207Pb/206Pb ages for zircons >1000 Ma.

Discussion

Potential Volcanic Sources of Basilika Formation Bentonites

Due to stratigraphic constraints, the interval of ~62−58 Ma is a realistic estimate for the depositional age of the Basilika Formation and the volcanic ashes. This volcanic activity predates the main phase of the NALIP around 55−50 Ma, which produced the ash layers widespread in the North Atlantic region (Figure 1; Tsikalas et al., 2002; Larsen et al., 2003a; Storey et al., 2007; Tegner et al., 2011), but it is temporally related to the initial phase of the NALIP at around 61 Ma and several alkaline volcanic events in the high Arctic (Figure 1).

The initial phase of the NALIP is expressed mainly as tholeiitic intrusives and flood basalts on the British Isles, East Greenland, Baffin Island and West Greenland including Disko Island, and is related to continental rifting to the east and west of Greenland (Storey et al., 2007). The REE patterns of the Basilika Formation bentonites show no resemblance to those of the tholeiites, but they fit well to the REE signatures of alkaline basalts from Disko Island (Figure 7; Larsen et al., 2003b; Larsen and Pedersen, 2009). However, the NALIP is unlikely to have sourced the Basilika Formation bentonites as the initial phase of the NALIP was not commonly associated with explosive activity (O'Nions and Clarke, 1972; Thompson, 1982; Storey et al., 1998; Larsen and Pedersen, 2009). The only evidence for early Paleocene explosive volcanism related to the NALIP are ~58 Ma old basalt tuffs from the Svartenhuk Formation in the Nuussuaq basin of western Greenland. However, the REE patterns of the Svartenhuk Formation basalts (Larsen et al., 2016) do not resemble those of the bentonites from the Basilika and Mount Lawson formations.

Instead, some of the REE patterns of the Basilika Formation bentonites correlate relatively well with those of Lawson-ash 1, which was deposited on southern Ellesmere Island at ~60 Ma (Figure 7; Reinhardt et al., 2013), both showing steep REE patterns with strong enrichment in LREE over HREE and small negative Eu anomalies. Additionally, Lawson-ash 1 and the Basilika Formation bentonites show broadly similar major element composition but some differences in MgO, Na2O, and SiO2 contents (Table 2), which may have been caused by different degrees of alteration.

The REE patterns of some of the Basilika Formation bentonites as well as Lawson-ash 1 broadly resemble those of the evolved members of the Kap Washington Group on North Greenland as well as volcanic detritus in the Cape Back Basin near Nares Strait on Ellesmere Island (Estrada et al., 2010; Thorarinsson et al., 2011a). The Kap Washington Group comprises a 5000 m thick suite of bimodal, basaltic to rhyolitic rocks, which was emplaced between 71 and 61 Ma (Brown et al., 1987; Estrada et al., 2001; Tegner et al., 2011; Thorarinsson et al., 2011a,b). The evolved phase of the Kap Washington Group was associated with explosive volcanism producing tuffs, ignimbrites, and pyroclastic sandstones (Brown et al., 1987; Thorarinsson et al., 2011a) and may potentially have sourced part of the bentonites on Svalbard and Ellesmere Island. In this case, the time of deposition of Lawson-ash 1 would need to coincide with the last volcanic activity on northern Greenland, which can be reconciled only if the maximum errors of age determinations are considered (Reinhardt et al., 2013). Moreover, the initial εNd(t) values of Lawson-ash 1 [εNd(60) = 2.9] exclude a provenance from the evolved phase of the Kap Washington Group [εNd(70) < 1]. Similarly, the εNd(60) values of the Basilika Formation bentonites (0.3−1.6) are higher than or within the upper range of the most positive εNd(t) values observed in evolved rocks of the Kap Washington Group (Estrada and Henjes-Kunst, 2004; Thorarinsson et al., 2011a).

The alkaline volcanic detritus from the Cape Back basin, originating from ignimbrites and lava flows produced between 61 and 58 Ma, exhibits REE patterns that resemble those of Lawson-ash 1 and parts of the Basilika Formation bentonites (CASE 1 samples FTS35-36) including the lack of a negative Eu anomaly (Figure 7; Estrada et al., 2010). Additionally, the εNd(t) values of both Lawson ash 1 and the Basilika Formation bentonites fall into the wide range of εNd(t) values of the Cape Back basin detritus. Given the close temporal and paleogeographic proximity, it is plausible that the volcanic detritus of the Cape Back basin and parts of the bentonite layers from Svalbard and Ellesmere Island share a common, alkaline, continental rift-related source and potentially originate from the same volcanic center (Estrada et al., 2010).

The dating of Lawson-ash 2 from Ellesmere Island was associated with relatively high uncertainties, but if the preliminary age of 53.90 ± 3.1 Ma (Reinhardt et al., 2013) is correct, it would postdate the Basilika Formation bentonites and the youngest known alkaline volcanic suite in the High Arctic at Bathurst Island (~56 Ma; Day et al., 2005). The Lawson-ash 2 bentonite layer shows significantly less enrichment in LREE (Figure 7) and seems geochemically and temporally related to the later, major phase of the NALIP. Similar to coeval ash deposits in the North Atlantic Ocean (Figure 1; cf. Larsen et al., 2003a), this ash may have emanated from volcanic centers in eastern Greenland (Heister et al., 2001) or western Greenland (Thompson, 1975; Saunders et al., 1997; Larsen et al., 2016), and might be causally linked to the occurrence of early Eocene bentonites in the Frysjaodden Formation in the CTB of Svalbard (cf. Charles et al., 2011).

In conclusion, the Paleocene bentonites on Svalbard and Ellesmere Island fit well into the emerging view of widespread continental rift-related alkaline volcanism in the Canadian High Arctic and North Greenland that predates the almost simultaneous start of spreading in the Eurasia Basin, Baffin Bay, and the North Atlantic Ocean. This volcanism was possibly originally of a larger extent than it can be assumed from the preserved volcanic centers, i.e., the outcrops of the ca. 80 Ma old Hansen Point Volcanic Complex on northwestern Ellesmere Island (Estrada and Henjes-Kunst, 2004, 2013) and the ~71−61 Ma old Kap Washington Group of North Greenland (Tegner et al., 2011; Thorarinsson et al., 2011b). This volcanic phase is furthermore recorded by the ~61−58 Ma old volcanic detritus in Paleocene basins (Cape Back Basin) on northeastern Ellesmere Island (Figure 1; Estrada et al., 2010) and ~58 Ma old tuffs in the Nuussuaq basin in western Greenland (Larsen et al., 2016).

Provenance of Detrital Zircons in the Basilika Formation

Potential Sources of Detrital Zircons in the Basilika Formation

The dominant zircon age populations of the Basilika Formation bentonites imply contributions of cratonic sources to the Paleoproterozoic (1800−1900 Ma) and the smaller Neoarchean (2700−2800 Ma) populations, as well as from Uralian, Caledonian and Timanian sources and probably the Siberian trap volcanism to the 200−650 Ma population. A characteristic feature of the Basilika Formation is the almost complete lack of Grenville-aged and older Mesoproterozoic-aged grains (apart from a small early Neoproterozoic population of 900−1000 Ma).

Rocks with Caledonian, late Grenvillian and Paleoproterozoic to Archean ages are exposed today on northern and westernmost Svalbard (Figure 2). Northern Svalbard has experienced continuous erosion during the Jurassic to Cretaceous, followed by fault-related Late Cretaceous to Early Paleocene exhumation and erosion mainly in NE Spitsbergen. Thus, northern Svalbard potentially shed detritus toward the south during the Paleocene (Dörr et al., 2012). Potential cratonic sources in western Ny Friesland comprise ca. 1750 Ma old granitic orthogneisses, 2709 ± 28 Ma old quartz-monzonite and metasediments with Paleoproterozoic (1870−2040 Ma) and Neoarchean detrital zircon ages (Hellman et al., 1997, 2001). Detrital zircons from another related metasedimentary unit, the Smutsbreen Formation of southwestern Ny Friesland, yielded single zircon Pb-evaporation plateau ages of 2560−2680 Ma, but also of ca. 1200−1300 and 1560−1710 Ma (Gee and Hellman, 1996), i.e., in a range that is not typical for the Basilika age spectrum. Caledonian granitoids, known from Nordaustlandet and the Northwestern Basement Province, can contribute 410−450 Ma old zircons. Further, Grenvillian granites, known from Nordaustlandet and the Northwestern and Southwestern Basement provinces, were intruded at ca. 930−960 Ma (e.g., Johansson et al., 2004, 2005; Gasser, 2014, references therein). However, both the Grenvillian and Caledonian granites have intruded metasedimentary rocks with abundant zircon ages in the range of 1000−1800 Ma (e.g., Pettersson et al., 2009, 2010; Lorenz et al., 2012; Gasser and Andresen, 2013). A selective erosion of the granitoids without the country rocks is very unlikely, unless such an intrusive body has experienced a stronger exhumation as part of a fault-bounded block.

Reworking of Mesozoic sediments surrounding the CTB may represent an alternative source for the detrital zircons in the Basilika Formation. Mesozoic sediments have covered the whole of Svalbard up to the onset of uplift of northern Svalbard and the formation of the West Spitsbergen Fold-and-Thrust Belt (e.g., Smelror et al., 2009). These rocks also covered large areas of the northern and north-eastern Barents Shelf, where uplift and erosion took place probably already since the end of the Early Cretaceous, expressed by a regional unconformity between Aptian-Albian and Paleocene strata and missing Upper Cretaceous sediments on Svalbard (e.g., Smelror et al., 2009; Dallmann, 2015). Mesozoic sediments exposed in central and southern Svalbard comprise Triassic to Lower Cretaceous strata. Detrital zircon age spectra of these sediments, reported by Pózer Bue and Andresen (2014), differ strongly from those of the Basilika Formation. The characteristic 1800−1900 and 2700−2800 Ma populations of the Basilika Formation are absent or only scarcely present in Late Triassic and Early Jurassic formations. Instead these formations are dominated by zircon ages in the range of 200−500 Ma. In contrast, the other Mesozoic formations contain the 1800−1900 and 2700−2800 Ma age populations, but additionally abundant 1100−1600 Ma zircon ages, which are not typical for the Basilika Formation. In summary, reworking of and mixing between Mesozoic formations of Svalbard combined with sediment input from uplifting Caledonian and pre-Caledonian sources in northern Svalbard cannot produce the zircon age spectrum of the Basilika Formation.

Another possibility is a western provenance as indicated by similarities between the detrital zircon age spectra of the Basilika Formation (Figure 10) and the Mount Lawson Formation from southern Ellesmere Island (Figure 11). The source area for the Mesoproterozoic to Neoarchean zircons in the Mount Lawson Formation is presumably the Canadian-Greenland Shield. However, similar to the cratonic rocks of North Svalbard, the Canadian-Greenland Shield provides not only Neoarchean to Paleoproterozoic zircon ages, but also abundant zircon ages in the range of ca. 1000−1500 Ma (Røhr et al., 2008; Kirkland et al., 2009), which in turn rarely occur in the Basilika Formation. This makes a westerly source of the Basilika sediments unlikely, and points toward an easterly provenance (Figure 12).

FIGURE 12
www.frontiersin.org

Figure 12. Paleogeography of Svalbard (A) and the surrounding regions (B) during the Paleocene before the onset of seafloor spreading in the Eurasia Basin, North Atlantic and Baffin Bay (A: after Worsley, 1986; B: after Scotese, 2001; Torsvik et al., 2002; Coward et al., 2003; Gee et al., 2006; Omma et al., 2011; Seton et al., 2012; Piepjohn et al., 2013). Red arrows show inferred provenance of detrital zircons. Sampling location indicated by white cross in (A). For further explanation see discussion in the text.

Surprisingly, the best fit is with detrital zircon age spectra of sediments from northern Siberia, which are exposed in the Verkhoyansk Fold-and-Thrust Belt, the South Anyui Zone, Chukotka, and the New Siberian Stolbovoi Island (Miller et al., 2006, 2008; Prokopiev et al., 2008; Soloviev and Miller, 2014). The Verkhoyansk Fold-and-Thrust Belt contains a 15-km-thick Carboniferous to Jurassic sequence that was deposited along the eastern passive margin of the Siberian craton and deformed during the collision with the Kolyma-Omolon superterrane in the Late Jurassic (Prokopiev et al., 2008). Late Carboniferous to Middle Jurassic sediments from Verkhoyansk show detrital zircon age spectra that are characterized by populations from 250 to 700 Ma (with peaks at around 300, 400, and 480−500 Ma), from 1800 to 2100 Ma, a small population from ca. 2400 to 2800 Ma, and a hiatus between 900 and 1600 Ma (Miller et al., 2006; Prokopiev et al., 2008). The Middle Jurassic sediments bear additional small populations with peaks at 176 and 229 Ma (Prokopiev et al., 2008). Late Jurassic to Early Cretaceous sediments from the South Anyui Zone, Stolbovoi Island and Chukotka have very similar zircon age spectra (Miller et al., 2008). The 250−330 Ma ages, the early Paleozoic ages and the Paleoproterozoic ages in the Verkhoyansk sediments can be linked to intrusive rocks in mountain belts in the Baikal region, from where the detritus was transported by large river systems toward the Verkhoyansk passive margin (Miller et al., 2006; Prokopiev et al., 2008). The youngest ages can be correlated with the Main Granitoid Belt of the Verkhoyansk Fold-and-Thrust Belt formed during collision-related arc magmatism between 143 and 160 Ma (U-Pb SHRIMP zircon data; Akinin et al., 2009). These ages fit also well with the youngest ages of the Basilika Formation age spectrum. However, how likely is sediment transport from such remote areas to Svalbard over a distance of about 3000 km during the Paleocene?

Sediment Transport Pathways in the Arctic during the Early Paleocene

For the present-day Arctic configuration, coarse-clastic sediment transport from the river mouths along the Siberian coast toward the Fram Strait is possible by sea ice, following the Transpolar Drift (Krylov et al., 2008; Thompson et al., 2012). However, perennial sea ice cover and current conditions including the Beaufort Gyre and the Transpolar Drift were likely established during the Miocene (Krylov et al., 2008; Thompson et al., 2012). During the Paleogene, the Arctic Ocean was a much more enclosed basin with only restricted exchange toward the North Atlantic (Thompson et al., 2012). There is, however, increasing evidence for earlier Arctic glaciation periods (e.g., Moran et al., 2006; Tripati et al., 2008; Immonen, 2013), and the Basilika Formation contains erratics, glendonite (a cold climate indicator), as well as dropstones (Spielhagen and Tripati, 2009, and own field observations), which suggests episodic cold periods with at least seasonal sea ice, intermittent with warmer periods (Spielhagen and Tripati, 2009). Thus, transport of the Basilika detritus from Siberia toward the west by sea ice following similar pathways as today cannot be completely ruled out, but the observed phenomena may hint also to a seasonal, more local ice transport.

Another option would be a transport by (possibly alongshore) currents, which redistributed sediments from Siberia toward the Paleocene position of Svalbard, then still located somewhere north of Greenland (Figure 12). Little is known about the current system at that time. Sediment pathways may have followed the area between the rising northern edge of the Barents Shelf and the Lomonosov Ridge. The latter was presumably exposed above sea level during the Paleocene and Late Cretaceous, as indicated by a pronounced unconformity between ca. 80 and 56 Ma (O'Regan et al., 2008 and references therein), and thus formed a barrier for sediment currents from the Siberian coastal areas against the Amerasia Basin (Figure 12B). However, this scenario appears unlikely as the uplift of the northern edge of the Barents Shelf would also prohibit sediment transport toward the CTB in the South-West.

A third possibility is that the Basilika Formation clastics of “Siberian origin” were transported to the CTB in several steps including intermediate storage in Mesozoic sediments of the northeastern Barents Shelf. Indeed, an easterly (Uralian and Timanian) provenance has been suggested earlier for Paleozoic detrital zircons in Late Triassic strata on Svalbard and in the Sverdrup Basin (Pózer Bue and Andresen, 2014; Anfinson et al., in press). In this context it should be noted that (i) Mesozoic sediments exposed east of Svalbard (Franz Josef Land) display different detrital age patterns than those exposed on Svalbard, and do NOT contain the Grenvillian ages characteristic for the “westerly” provenance of most of the Svalbardian Mesozoic sediments (Soloviev et al., 2015); and (ii) that Mesozoic sediments of the Barents Sea underwent extensive erosion during the Paleocene, as evidenced, amongst others, by Triassic, Jurassic and Early Cretaceous sediments subcropping over wide areas of the northeastern Barents Shelf beneath the actual seafloor (e.g., Asch, 2005).

Thus, Mesozoic sediments originally sourced from the Verkhoyansk Fold-and-Thrust Belt and mixed with clastic detritus derived from the Siberian traps, the Uralides and the Timanides may have been reworked and redeposited during the Paleocene (Figure 12B). However, a convincing answer regarding transport mechanisms across the Arctic including larger scale fluvial drainage patterns will only be possible when more data become available, both on the provenance of clastic sediments and the Paleogene climate evolution of the Arctic.

In any case, it is striking that the Basilika Formation apparently received only little detritus from the immediate surroundings, including the Mesozoic sediments presently exposed directly east of the CTB, the area of the present West Spitsbergen Fold-and-Thrust Belt toward the west, and northern Svalbard, which was emergent and underwent erosion during the Paleocene (Dörr et al., 2012). Only the small late Grenvillian age group contained in the Basilika sediments seems to be derived from local sources, most likely from the Newtontoppen area toward the north, which was relatively rapidly exhumed during the Paleocene (Dörr et al., 2012; the Newtontoppen is the highest peak of present-day Svalbard, consisting of a Caledonian granitic body intruded into Proterozoic metamorphic rocks). The paucity of local detritus implies that the West-Spitsbergen Fold-and-Thrust Belt was still not active, in agreement with previous assumptions (Tessensohn and Piepjohn, 2000), and that the Mesozoic cover, today exposed east of the CTB, was still an area of deposition rather than of erosion. Higher subsidence rates occurred in the Eocene, when the West Spitsbergen Fold-and-Thrust Belt became active, and sediment transport changed from an easterly to a westerly source area (Helland-Hansen, 1990; Bruhn and Steel, 2003). The lack of local detritus also implies that the contribution from North Svalbard was either minor and thus strongly diluted by the dominant eastern source (in agreement with relatively low erosion rates reported for North Svalbard; Dörr et al., 2012), or that North Svalbard was drained toward the North into the assumed lowland between Svalbard and the Lomonosov Ridge, with the local drainage divide presumably located in the Newtontoppen area.

Conclusions

In this study we investigated the characteristics of bentonite layers contained in the Paleocene Basilika Formation, as well as the provenance of their clastic host rocks. Bentonite layers were sampled from the lower and upper parts of the Basilika Formation in the Bjørndalen area on central Spitsbergen. For geochemical comparisons, additional bentonite samples from the Basilika Formation taken during the CASE 1 expedition of BGR in 1992 and two samples from the Lower Paleogene Mount Lawson Formation of Ellesmere Island (Canadian Arctic) were included.

From our data we draw the following conclusions:

(i) The four analyzed bentonite layers from Bjørndalen represent altered volcanic ashes that originate from a common mantle source, but with different degrees of partial melting and having experienced different fractionation. The older layers are less evolved than the younger layers and were derived from an alkali-basaltic parental magma, whereas the younger layers were derived from a trachytic to alkali-rhyolitic precursor.

(ii) The geochemical fingerprints of the CASE 1 bentonite samples show similarities with, but also differences to, the Bjørndalen bentonites, which renders an origin of all Basilika bentonites from a common volcanic center unlikely. However, some of the CASE 1 samples may share a common source with the volcanic detritus from the Nares Strait area (Estrada et al., 2010).

(iii) The Basilika Formation bentonites, the ~60 Ma bentonite layer on Ellesmere Island (Lawson-ash 1; Reinhardt et al., 2013) and the 61–58 Ma volcanic detritus in the Nares Strait area (Estrada et al., 2010) all originate from alkaline, continental-rift magmatism related to the last, explosive stages of the HALIP. This magmatism was probably more widespread in the Arctic during the Paleocene than it can be assumed from the present-day extent of volcanites (e.g., the 71−61 Ma Kap Washington Group of North Greenland; Tegner et al., 2011; Thorarinsson et al., 2011b). Other volcanic centers may have been eroded or remain hidden beneath ice caps.

(iv) All Bjørndalen bentonite layers contain detrital zircons with four distinct U–Pb age groups of Neoarchean (2800−2700 Ma), Paleoproterozoic (1900−1800 Ma), late Grenvillian (1000−900 Ma), and Neoproterozoic/Phanerozoic age (650−200 Ma). The constant zircon age patterns indicate that the clastic sediments hosting the bentonite layers originated from the same source over the whole time of deposition of the Basilika Formation.

(v) The Grenvillian age group is very small, thus excluding a significant input from local sources or from westerly sources and pointing to a predominantly eastern provenance. The most important source seems to have been the Cretaceous Verkhoyansk Fold-and-Thrust Belt exposed in Siberia more than 3000 km away from Svalbard.

(vi) Several sediment transport mechanism are conceivable, such as ice rafting or alongshore currents following the northern edge of the Eurasian continental margin. Also, multi-stage sediment transport including intermediate storage and later reworking of the Siberian detritus in Mesozoic sediments may explain the zircon age signature of the Basilika Formation. Further provenance studies on different stratigraphic layers and locations across the Arctic are required to gain a better understanding of Paleocene sediment pathways, current systems, fluvial drainage systems, and transport mechanisms.

Author Contributions

FE, CS, SE, FL designed research; FE, SE, DD, LR, FH, NA, RD performed research; FE, CS, SE, DD, LR, FH, RD, KP analyzed data; and FE, CS, SE wrote the paper with input from all co-authors.

Conflict of Interest Statement

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

Acknowledgments

We thank Franz Tessensohn and Hans Paech for providing information on CASE 1 bentonite samples. Lotte M. Larsen and Fernando Corfu are thanked for providing comments that improved this manuscript.

Supplementary Material

The Supplementary Material for this article can be found online at: https://www.frontiersin.org/article/10.3389/feart.2016.00073

References

Akinin, V. V., Prokopiev, A. V., Toro, J., Miller, E. L., Wooden, J., Goryachev, N. A., et al. (2009). U–Pb SHRIMP ages of granitoides from the main batholith belt (North East Asia). Dokl. Earth Sci. 426, 605–610. doi: 10.1134/S1028334X09040217

CrossRef Full Text | Google Scholar

Anfinson, O. A., Embry, A. F., and Stockli, D. F. (in press). Geochronologic constraints on the permian-triassic northern source region of the sverdrup basin, Canadian Arctic Islands. Tectonophysics. doi: 10.1016/j.tecto.2016.02.041

CrossRef Full Text | Google Scholar

Asch, K. (2005). The 1:5 Million International Geological Map of Europe and Adjacent Areas - IGME 5000. Hannover: BGR.

Bergh, S. G., Braathen, A., and Andresen, A. (1997). Interaction of basement-involved and thin-skinned tectonism in the tertiary fold-thrust belt of central Spitsbergen, Svalbard. Am. Assoc. Pet. Geol. Bull. 81, 637–661.

Google Scholar

Blythe, A. E., and Kleinspehn, K. L. (1998). Tectonically versus climatically driven Cenozoic exhumation of the Eurasian plate margin, Svalbard: Fission track analyses. Tectonics 17, 621. doi: 10.1029/98TC01890

CrossRef Full Text | Google Scholar

Braathen, A., Bergh, S. G., and Maher, H. D. (1999). Application of a critical wedge taper model to the Tertiary transpressional fold-thrust belt on Spitsbergen, Svalbard. Geol. Soc. Am. Bull. 111, 1468–1485.

Google Scholar

Brown, P. E., Parsons, I., and Becker, S. M. (1987). Peralkaline volcanicity in the Arctic Basin-the Kap Washington Volcanics, petrology and palaeotectonics. J. Geol. Soc. Lond. 144, 707–715. doi: 10.1144/gsjgs.144.5.0707

CrossRef Full Text | Google Scholar

Bruhn, R., and Steel, R. J. (2003). High-resolution sequence stratigraphy of a clastic foredeep succession (Paleocene, Spitsbergen): an example of peripheral-bulge-controlled depositional architecture. J. Sediment. Res. 73, 745–755. doi: 10.1306/012303730745

CrossRef Full Text | Google Scholar

Buchan, K. L., and Ernst, R. E. (2006). “Giant dyke swarms and the reconstruction of the Canadian Arctic Islands, Greenland, Svalbard and Franz Josef Land,” in Dyke Swarms: Time Markers of Crustal Evolution, eds E. Hanski, S. Mertanen, T. Rämö, and J. Vuollo (Balkema: Taylor & Francis), 27–48.

Google Scholar

CASE Team (2001). “The evolution of the west spitsbergen fold-and-thrust belt,” in Intra-Continental Fold Belts CASE 1: West Spitsbergen, ed F. Tessensohn (Stuttgart: E. Schweizerbart'sche Verlagsbuchhandlung), 733–773.

Cavalcante, F., Belviso, C., Piccarreta, G., and Fiore, S. (2014). Grain-size control on the rare earth elements distribution in the late diagenesis of Cretaceous shales from the Southern Apennines (Italy). J. Chem. 2014:841747. doi: 10.1155/2014/841747

CrossRef Full Text | Google Scholar

Čepek, P. (2001). “Paleogene calcareous nannofossils from the firkanten and sarsbukta formations on Spitsbergen,” in Intra-Continental Fold Belts CASE 1: West Spitsbergen, ed F. Tessensohn (Stuttgart: E. Schweizerbart'sche Verlagsbuchhandlung), 535–547.

Čepek, P., and Krutzsch, W. (2001). “Conflicting interpretations of the Tertiary biostratigraphy of Spitsbergen and new palynological results,” in Intra-Continental Fold Belts CASE 1: West Spitsbergen, ed F. Tessensohn (Stuttgart: E. Schweizerbart'sche Verlagsbuchhandlung), 551–599.

Charles, A. J., Condon, D. J., Harding, I. C., Pälike, H., Marshall, J. E. A., Cui, Y., et al. (2011). Constraints on the numerical age of the Paleocene–Eocene boundary. Geochem. Geophys. Geosyst. 12, Q0AA17. doi: 10.1029/2010GC003426

CrossRef Full Text | Google Scholar

Christidis, G. E. (1998). Comparative study of the mobility of major and trace elements during alteration of an andesite and a rhyolite to bentonite, in the Islands of Milos and Kimolos, Aegean, Greece. Clays Clay Miner. 46, 379–399. doi: 10.1346/CCMN.1998.0460403

CrossRef Full Text | Google Scholar

Corfu, F., Polteau, S., Planke, S., Faleide, J. I., Svensen, H., Zayoncheck, A., et al. (2013). U-Pb geochronology of Cretaceous magmatism on Svalbard and Franz Josef Land, Barents Sea Large Igneous Province. Geol. Mag. 150, 1127–1135. doi: 10.1017/S0016756813000162

CrossRef Full Text | Google Scholar

Coward, M. P., Dewey, J., Hempton, M., and Holroyd, J. (2003). “Tectonic evolution,” in The Millennium Atlas: Petroleum Geology of the Central and Northern North Sea, eds D. Evans, C. Graham, A. Armour, and P. Bathurst (London: Geological Society), 17–33.

Dallmann, W. K. (1999). Lithostratigraphic Lexicon of Svalbard. Tromsø: Norsk Polarinstitutt.

Dallmann, W. K. (2015). Geoscience Atlas of Svalbard. Tromsø: Norsk Polarinstitutt.

Day, J. M. D., Hilton, D. R., Pearson, D. G., Macpherson, C. G., Kjarsgaard, B. A., and Janney, P. E. (2005). Absence of a high time-integrated 3He/(U+Th) source in the mantle beneath continents. Geology 33, 733–736. doi: 10.1130/G21625.1

CrossRef Full Text | Google Scholar

Dohrmann, R., Genske, D., Karnland, O., Kaufhold, S., Kiviranta, L., Olsson, S., et al. (2012). Interlaboratory CEC and exchangeable cation study of bentonite buffer materials: I. Cu(II)-triethylenetetramine method. Clays Clay Miner. 60, 162–175. doi: 10.1346/CCMN.2012.0600206

CrossRef Full Text | Google Scholar

Dörr, N., Clift, P. D., Lisker, F., and Spiegel, C. (2013). Why is Svalbard an island? Evidence for two-stage uplift, magmatic underplating, and mantle thermal anomalies. Tectonics 32, 1–14. doi: 10.1002/tect.20039

CrossRef Full Text

Dörr, N., Lisker, F., Clift, P. D., Carter, A., Gee, D. G., Tebenkov, A. M., et al. (2012). Late Mesozoic–Cenozoic exhumation history of northern Svalbard and its regional significance: constraints from apatite fission track analysis. Tectonophysics 514–517, 81–92. doi: 10.1016/j.tecto.2011.10.007

CrossRef Full Text

Døssing, A., Hopper, J. R., Olesen, A. V., Rasmussen, T. M., and Halpenny, J. (2013a). New aero-gravity results from the Arctic: linking the latest Cretaceous-early Cenozoic plate kinematics of the North Atlantic and Arctic Ocean. Geochem. Geophys. Geosystems 14, 4044–4065. doi: 10.1002/ggge.20253

CrossRef Full Text

Døssing, A., Jackson, H. R., Matzka, J., Einarsson, I., Rasmussen, T. M., Olesen, A. V., et al. (2013b). On the origin of the Amerasia basin and the high arctic large igneous province—Results of new aeromagnetic data. Earth Planet. Sci. Lett. 363, 219–230. doi: 10.1016/j.epsl.2012.12.013

CrossRef Full Text | Google Scholar

Døssing, A., Japsen, P., Watts, A. B., Nielsen, T., Jokat, W., Thybo, H., et al. (2016). Miocene uplift of the NE Greenland margin linked to plate tectonics: seismic evidence from the Greenland Fracture Zone, NE Atlantic. Tectonics 35, 257–282. doi: 10.1002/2015TC004079

CrossRef Full Text | Google Scholar

Dypvik, H., and Nagy, J. (1978). Early tertiary bentonites frorn Svalbard; a Preliminary Report. Polarforschung 48, 139–150.

Google Scholar

Embry, A. F., and Osadetz, K. G. (1988). Stratigraphy and tectonic significance of Cretaceous volcanism in the Queen Elizabeth Islands, Canadian Arctic Archipelago. Can. J. Earth Sci. 25, 1209–1219. doi: 10.1139/e88-118

CrossRef Full Text | Google Scholar

Estrada, S. (2015). Geochemical and Sr-Nd isotope variations within Cretaceous continental flood-basalt suites of the Canadian High Arctic, with a focus on the Hassel Formation basalts of northeast Ellesmere Island. Int. J. Earth Sci. 104, 1981–2005. doi: 10.1007/s00531-014-1066-x

CrossRef Full Text | Google Scholar

Estrada, S., and Henjes-Kunst, F. (2004). Volcanism in the Canadian high arctic related to the opening of the Arctic Ocean. Zeitschrift Dtsch. Geol. Gesellschaft 154, 579–604.

Google Scholar

Estrada, S., and Henjes-Kunst, F. (2013). 40Ar-39Ar and U-Pb dating of Cretaceous continental rift-related magmatism on the northeast Canadian Arctic margin. Zeitschrift Dtsch. Gesellschaft Geowissenschaften 164, 107–130. doi: 10.1127/1860-1804/2013/0005

CrossRef Full Text | Google Scholar

Estrada, S., Henjes-Kunst, F., Melcher, F., and Tessensohn, F. (2010). Paleocene alkaline volcanism in the Nares Strait region: evidence from volcanic pebbles. Int. J. Earth Sci. 99, 863–890. doi: 10.1007/s00531-009-0432-6

CrossRef Full Text | Google Scholar

Estrada, S., Höhndorf, A., and Henjes-Kunst, F. (2001). Cretaceous/Tertiary volcanism in North Greenland: the Kap Washington Group. Polarforschung 69, 17–23. doi: 10013/epic.29823.d001

CrossRef Full Text | Google Scholar

Faleide, J. I., Vågnes, E., and Gudlaugsson, S. T. (1993). Late Mesozoic–Cenozoic evolution of the southwestern Barents Sea in a regional riftshear tectonic setting. Pet. Geol. Conf. Ser. 4, 933–950.

Frisch, T., and Dawes, P. R. (2014). The rotations opening the Central and Northern Atlantic Ocean: compilation, drift lines, and flow lines. Int. J. Earth Sci. 103, 967–969. doi: 10.1007/s00531-013-0980-7

CrossRef Full Text | Google Scholar

Gaina, C., Gernigon, L., and Ball, P. (2009). Palaeocene-recent plate boundaries in the NE Atlantic and the formation of the Jan Mayen microcontinent. J. Geol. Soc. Lond. 166, 601–616. doi: 10.1144/0016-76492008-112

CrossRef Full Text | Google Scholar

Gaina, C., Nikishin, A. M., and Petrov, E. I. (2015). Ultraslow spreading, ridge relocation and compressional events in the East Arctic region: a link to the Eurekan orogeny? Arktos 1, 16. doi: 10.1007/s41063-015-0006-8

CrossRef Full Text | Google Scholar

Gasser, D. (2014). The Caledonides of Greenland, Svalbard and other arctic areas: status of research and open questions. Geol. Soc. Lond. Spec. Publ. 390, 93–129. doi: 10.1144/SP390.17

CrossRef Full Text | Google Scholar

Gasser, D., and Andresen, A. (2013). Caledonian terrane amalgamation of Svalbard: detrital zircon provenance of Mesoproterozoic to Carboniferous strata from Oscar II Land, western Spitsbergen. Geol. Mag. 150, 1103–1126. doi: 10.1017/S0016756813000174

CrossRef Full Text | Google Scholar

Gee, D. G., Bogolepova, O. K., and Lorenz, H. (2006). The timanide, caledonide and uralide orogens in the eurasian high arctic, and relationships to the palaeo-continents Laurentia, Baltica and Siberia. Geol. Soc. Mem. 32, 507–520. doi: 10.1144/GSL.MEM.2006.032.01.31

CrossRef Full Text | Google Scholar

Gee, D. G., and Hellman, F. (1996). Zircon Pb-evaporation ages from the smutsbreen formation, southern Ny Friesland: new evidence for Caledonian thrusting in Svalbard's Eastern Terrane. Zeitschrift Geol. Wissenschaften 24, 429–439.

Google Scholar

González López, J. M., Bauluz, B., Yuste, A., Mayayo, M. J., and Fernández-Nieto, C. (2005). Mineralogical and trace element composition of clay-sized fractions from Albian siliciclastic rocks (Oliete Basin, NE Spain). Clay Miner. 40, 565–580. doi: 10.1180/0009855054040193

CrossRef Full Text | Google Scholar

Gradstein, F. M., Ogg, J. G., Schmitz, M. D., and Ogg, G. M. (2012). The Geologic Time Scale, Vol. 2. Oxford: Elsevier.

Google Scholar

Greiner, B., and Neugebauer, J. (2013). The rotations opening the Central and Northern Atlantic Ocean: compilation, drift lines, and flow lines. Int. J. Earth Sci. 102, 1357–1376. doi: 10.1007/s00531-012-0860-6

CrossRef Full Text | Google Scholar

Gripp, K. (1927). Beiträge zur Geologie von Spitzbergen. Abhandlungen Naturwissenschaftlichen Vereins Hambg. 21, 1–38.

Grist, A. M., and Zentilli, M. (2004). Preliminary apatite fission track thermal history modelling of the nares strait region of Eastern Ellesmere Island and Northwestern Greenland. Polarforschung 74, 113–127.

Google Scholar

Harland, B. W. (1969). “Contribution of Spitsbergen to understanding of the tectonic evolution of the North Atlantic region,” in North Atlantic: Geology and Continental Drift. American Association of Petroleum Geologists Memoir 12, ed M. Kay (Tulsa: American Association of Petroleum Geologists), 817–851.

Harland, W. B. (1997). Geology of Svalbard. London: Geological Society.

Google Scholar

Heister, L. E., O'Day, P. A., Brooks, C. K., Neuhoff, P. S., and Bird, D. K. (2001). Pyroclastic deposits within the East Greenland Tertiary flood basalts. J. Geol. Soc. London. 158, 269–284. doi: 10.1144/jgs.158.2.269

CrossRef Full Text | Google Scholar

Helland-Hansen, W. (1990). Sedimentation in paleogene foreland Basin, Spitsbergen. Am. Assoc. Pet. Geol. Bull. 74, 260–272. doi: 10.1306/0c9b22bd-1710-11d7-8645000102c1865d

CrossRef Full Text | Google Scholar

Hellman, F. J., Gee, D. G., Johansson, Å., and Witt-Nilsson, P. (1997). Single-zircon Pb evaporation geochronology constrains basement-cover relationships in the lower Hecla Hoek Complex of northern Ny Friesland, Svalbard. Chem. Geol. 137, 117–134. doi: 10.1016/S0009-2541(96)00152-0

CrossRef Full Text | Google Scholar

Hellman, F. J., Gee, D. G., and Witt-Nilsson, P. (2001). Late archean basement in the bangenhuken complex of the Nordbreen Nappe, western Ny-Friesland, Svalbard. Polar Res. 20, 49–59. doi: 10.1111/j.1751-8369.2001.tb00038.x

CrossRef Full Text | Google Scholar

Hopper, J. R., Dahl-Jensen, T., Holbrook, W. S., Larsen, H. C., Lizarralde, D., Korenaga, J., et al. (2003). Structure of the SE Greenland margin from seismic reflection and refraction data: implications for nascent spreading center subsidence and asymmetric crustal accretion during North Atlantic opening. J. Geophys. Res. 108, 2269. doi: 10.1029/2002JB001996

CrossRef Full Text | Google Scholar

Immonen, N. (2013). Surface microtextures of ice-rafted quartz grains revealing glacial ice in the Cenozoic Arctic. Palaeogeogr. Palaeoclimatol. Palaeoecol. 374, 293–302. doi: 10.1016/j.palaeo.2013.02.003

CrossRef Full Text | Google Scholar

Jackson, H. R., and Gunnarsson, K. (1990). Reconstructions of the Arctic: mesozoic to present. Tectonophysics 172, 303–322. doi: 10.1016/0040-1951(90)90037-9

CrossRef Full Text | Google Scholar

Johansson, A., Gee, D. G., Larionov, A. N., Ohta, Y., and Tebenkov, A. M. (2005). Grenvillian and Caledonian evolution of eastern Svalbard – a tale of two orogenies. Terra Nov. 17, 317–325. doi: 10.1111/j.1365-3121.2005.00616.x

CrossRef Full Text | Google Scholar

Johansson, A., Larionov, A. N., Gee, D. G., Ohta, Y., Tebenkov, A. M., and Sandelin, S. (2004). Grenvillian and Caledonian tectono-magmatic activity in northeasternmost Svalbard. Geol. Soc. Mem. 30, 207–232. doi: 10.1144/GSL.MEM.2004.030.01.17

CrossRef Full Text | Google Scholar

Jones, M., Burgess, S., Eliassen, G., Svensen, H., Planke, S., Jochmann, M., et al. (2015). Arctic volcanism during the Palaeocene and Eocene: the timing and provenance of volcanic ashes in the Central Tertiary Basin, Svalbard. Geophys. Res. Abstr. 17, EGU2015-11468.

Google Scholar

Jowitt, S. M., Williamson, M. C., and Ernst, R. E. (2014). Geochemistry of the 130 to 80 Ma Canadian high arctic large igneous province (HALIP) event and implications for Ni-Cu-PGE prospectivity. Econ. Geol. 109, 281–307. doi: 10.2113/econgeo.109.2.281

CrossRef Full Text | Google Scholar

Kirkland, C. L., Pease, V., Whitehouse, M. J., and Ineson, J. R. (2009). Provenance record from Mesoproterozoic-Cambrian sediments of Peary Land, North Greenland: implications for the ice-covered Greenland Shield and Laurentian palaeogeography. Precambrian Res. 170, 43–60. doi: 10.1016/j.precamres.2008.11.006

CrossRef Full Text | Google Scholar

Knox, R. W. O., and Morton, A. C. (1988). “The record of early Tertiary N Atlantic volcanism in sediments of the North Sea Basin,” in Early Tertiary Volcanism and the Opening of the NE Atlantic, eds A. C. Morton and L. M. Parson (London: Geological Society), 407–419.

Kontak, D. J., Jensen, S. M., Dostal, J., Archibald, D. A., and Kyser, T. K. (2001). Cretaceous mafic dyke swarm, Peary Land, northernmost Greenland: geochronology and petrology. Can. Mineral. 39, 997–1020. doi: 10.2113/gscanmin.39.4.997

CrossRef Full Text | Google Scholar

Kristoffersen, Y., and Talwani, M. (1977). Extinct triple junction south of Greenland and the Tertiary motion of Greenland relative to North America. Bull. Geol. Soc. Am. 88, 1037–1049.

Google Scholar

Krylov, A. A., Andreeva, I. A., Vogt, C., Backman, J., Krupskaya, V. V., Grikurov, G. E., et al. (2008). A shift in heavy and clay mineral provenance indicates a middle Miocene onset of a perennial sea ice cover in the Arctic Ocean. Paleoceanography 23:PA1S06. doi: 10.1029/2007PA001497

CrossRef Full Text | Google Scholar

Larsen, L. M., Fitton, J. G., and Pedersen, A. K. (2003a). Paleogene volcanic ash layers in the Danish Basin: compositions and source areas in the North Atlantic Igneous Province. Lithos 71, 47–80. doi: 10.1016/j.lithos.2003.07.001

CrossRef Full Text | Google Scholar

Larsen, L. M., and Pedersen, A. K. (2009). Petrology of the paleocene picrites and flood basalts on disko and nuussuaq, West Greenland. J. Petrol. 50, 1667–1711. doi: 10.1093/petrology/egp048

CrossRef Full Text | Google Scholar

Larsen, L. M., Pedersen, A. K., Sundvoll, B., and Frei, R. (2003b). Alkali picrites formed by melting of old metasomatized lithospheric mantle: manîtdlat member, vaigat formation, Palaeocene of West Greenland. J. Petrol. 44, 3–38. doi: 10.1093/petrology/44.1.3

CrossRef Full Text | Google Scholar

Larsen, L. M., Pedersen, A. K., Tegner, C., Duncan, R. A., Hald, N., and Larsen, J. G. (2016). Age of Tertiary volcanic rocks on the West Greenland continental margin: volcanic evolution and event correlation to other parts of the North Atlantic Igneous Province. Geol. Mag. 153, 487–511. doi: 10.1017/S0016756815000515

CrossRef Full Text | Google Scholar

Lawver, L. A., Müller, R. D., Srivastava, S. P., and Roest, W. (1990). “The opening of the Arctic Ocean,” in Geological History of the Polar Oceans: Arctic versus Antarctic, eds U. Bleil and J. Thiede (Dordrecht: Kluwer), 29–62.

Livšic, J. J. (1967). “Tretičnye otloženija zapadnoj časti archipelaga Špicbergen (Tertiary deposits in the western part of the Archipelago of Svalbard),” in Materialy po stratigrafii Špicbergena, ed V. N. Sokolov (Leningrad: NIIGA), 185–204.

Livšic, J. J. (1974). Paleogene deposits and the platform structure of Svalbard. Nor. Polarinstitutt Skr. 159, 1–50.

Lorenz, H., Gee, D. G., Larionov, A. N., and Majka, J. (2012). The Grenville–Sveconorwegian orogen in the high Arctic. Geol. Mag. 149, 875–891. doi: 10.1017/S0016756811001130

CrossRef Full Text | Google Scholar

Ludwig, K. R. (1991). ISOPLOT - a Plotting and Regression Program for Radiogenic-Isotope Data. USGS Open-File Report 91–445, US Geological Survey.

Maher, H. D. (2001). Manifestations of the Cretaceous high arctic large igneous Province in Svalbard. J. Geol. 109, 91–104. doi: 10.1086/317960

CrossRef Full Text | Google Scholar

Major, H., Haremo, P., Dallmann, W. K., Kjærnet, T., and Nøttvedt, A. (2001). Geological Map of Svalbard 1:100,000, Sheet C9G Adventdalen. Tromsø: Norwegian Polar Institute.

Google Scholar

Major, H., and Nagy, J. (1964). Geological Map of Svalbard C9G, Adventdalen, 1:100,000, Oslo: Norsk Polarinstitutt.

Major, H., and Nagy, J. (1972). Geology of the Adventdalen Map Area. (Tromsø: Norsk Polarinstitutt), 138.

Manum, S. (1962). Studies in the Tertiary flora of Spitsbergen with Notes on Tertiary Floras of Ellesmere Island, Greenland, and Iceland. (Tromsø: Norsk Polarinstitutt), 125.

Google Scholar

Manum, S. B., and Throndsen, T. (1986). Age of Tertiary formations on Spitsbergen. Polar Res. 4, 103–131. doi: 10.1111/j.1751-8369.1986.tb00526.x

CrossRef Full Text | Google Scholar

Miall, A. D. (1991). “Late Cretaceous and Tertiary basin development and sedimentation, Arctic Islands,” in Geology of the Innuitian Orogen and Arctic Platform of Canada and Greenland, ed H. P. Trettin (Ottawa: Geological Survey of Canada), 437–458.

Miller, E. L., Soloviev, A., Kuzmichev, A. G., G., Toro, J., and Tuchkova, M. (2008). Jurassic and Cretaceous foreland basin deposits of the Russian Arctic: Separated by birth of the Makarov Basin? Nor. J. Geol. 88, 201–226.

Google Scholar

Miller, E. L., Toro, J., Gehrels, G., Amato, J. M., Prokopiev, A., Tuchkova, M. I., et al. (2006). New insights into Arctic paleogeography and tectonics from U-Pb detrital zircon geochronology. Tectonics 25, TC3013. doi: 10.1029/2005TC001830

CrossRef Full Text | Google Scholar

Minakov, A., Mjelde, R., Inge, J., Flueh, E. R., Dannowski, A., and Keers, H. (2012). Mafic intrusions east of Svalbard imaged by active-source seismic tomography. Tectonophysics 518–521, 106–118. doi: 10.1016/j.tecto.2011.11.015

CrossRef Full Text | Google Scholar

Moran, K., Backman, J., Brinkhuis, H., Clemens, S. C., Cronin, T., Dickens, G. R., et al. (2006). The Cenozoic palaeoenvironment of the Arctic Ocean. Nature 441, 601–605. doi: 10.1038/nature04800

PubMed Abstract | CrossRef Full Text | Google Scholar

Müller, R. D., and Spielhagen, R. F. (1990). Evolution of the Central Tertiary Basin of Spitsbergen: towards a synthesis of sediment and plate tectonic history. Palaeogeogr. Palaeoclimatol. Palaeoecol. 80, 153–172. doi: 10.1016/0031-0182(90)90127-S

CrossRef Full Text | Google Scholar

Nagy, J. (1966). Preliminary report on the geology of Eastern Torell Land, Vestspitsbergen. Nor. Polarinstitut Arb. 1964, 69–72.

Neugebauer, J., and Greiner, B. (2014). Reply to: Frisch and Dawes (DOI 10.1007/s00531-013-0980-7) discussion on The rotations opening the Central and Northern Atlantic Ocean: compilation, drift lines, and flow lines (DOI 10.1007/s00531-012-0860-6). Int. J. Earth Sci. 103, 971–976. doi: 10.1007/s00531-013-0981-6

CrossRef Full Text | Google Scholar

O'Nions, R. K., and Clarke, D. B. (1972). Comparative trace element geochemistrys of Tertiary basalts from Baffin Bay. Earth Planet. Sci. Lett. 15, 436–446.

Google Scholar

O'Regan, M., Moran, K., Backman, J., Jakobson, M., Sangiorgi, F., Brinkhuis, H., et al. (2008). Mid-Cenozoic tectonic and paleoenvironmental setting of the central Arctic Ocean. Paleoceanography 23, PA1S20. doi: 10.1029/2007PA001559

CrossRef Full Text | Google Scholar

Oakey, G. N., and Chalmers, J. A. (2012). A new model for the Paleogene motion of Greenland relative to North America: plate reconstructions of the Davis Strait and Nares Strait regions between Canada and Greenland. J. Geophys. Res. Solid Earth 117, B10401. doi: 10.1029/2011jb008942

CrossRef Full Text | Google Scholar

Omma, J. E., Pease, V., and Scott, R. A. (2011). U-Pb SIMS zircon geochronology of Triassic and Jurassic sandstones on northwestern Axel Heiberg Island, northern Sverdrup Basin, Arctic Canada. Geol. Soc. Mem. 35, 559–566. doi: 10.1144/M35.37

CrossRef Full Text | Google Scholar

Pearce, J. A. (1996). “A user's guide to basalt discrimination diagrams,” in Geological Association of Canada Short Course Notes 12, ed D. A. Wyman (St. John's: Geological Association of Canada), 79–113.

Pettersson, C. H., Pease, V., and Frei, D. (2009). U–Pb zircon provenance of metasedimentary basement of the Northwestern Terrane, Svalbard: implications for the Grenvillian–Sveconorwegian orogeny and development of Rodinia. Precambrian Res. 175, 206–220. doi: 10.1016/j.precamres.2009.09.010

CrossRef Full Text | Google Scholar

Pettersson, C. H., Pease, V., and Frei, D. (2010). Detrital zircon U-Pb ages of Silurian-Devonian sediments from NW Svalbard: a fragment of Avalonia and Laurentia? J. Geol. Soc. Lond. 167, 1019–1032. doi: 10.1144/0016-76492010-062

CrossRef Full Text | Google Scholar

Philpotts, J., and Schnetzler, C. (1968). Europium anomalies and the genesis of basalt. Chem. Geol. 3, 5–13. doi: 10.1016/0009-2541(68)90009-0

CrossRef Full Text | Google Scholar

Piepjohn, K., Thiedig, F., and Manby, G. M. (2001). “Nappe-Stacking on Brøggerhalvøya, NW Spitsbergen,” in Intra-Continental Fold Belts. CASE 1: West Spitsbergen, Geologisches Jahrbuch (Polar Issue No. 7), ed F. Tessensohn (Stuttgart: E. Schweizerbart'sche Verlagsbuchhandlung), 55–79.

Piepjohn, K., von Gosen, W., Läufer, A., McClelland, W. C., and Estrada, S. (2013). Ellesmerian and Eurekan fault tectonics at the northern margin of Ellesmere Island (Canadian High Arctic). Zeitschrift Dtsch. Gesellschaft Geowissenschaften 164, 81–105. doi: 10.1127/1860-1804/2013/0007

CrossRef Full Text | Google Scholar

Pitman, W. C., and Talwani, M. (1972). Sea-Floor Spreading in the North Atlantic. Geol. Soc. Am. Bull. 83, 619. doi: 10.1130/0016-7606(1972)83[619:SSITNA]2.0.CO;2

CrossRef Full Text | Google Scholar

Pózer Bue, E., and Andresen, A. (2014). “Constraining depositional models in the Barents Sea region using detrital zircon U-Pb data from Mesozoic sediments in Svalbard,” in Sediment Provenance Studies in Hydrocarbon Exploration and Production Special Publications, eds R. A. Scott, H. R. Smyth, A. C. Morton, and N. Richardson (London: Geological Society), 261–279.

Prokopiev, A. V., Toro, J., Miller, E. L., and Gehrels, G. E. (2008). The paleo–Lena River — 200 m.y. of transcontinental zircon transport in Siberia. Geology 36, 699. doi: 10.1130/G24924A.1

CrossRef Full Text | Google Scholar

Reinhardt, L., Estrada, S., Andruleit, H., Dohrmann, R., Piepjohn, K., von Gosen, W., et al. (2013). Altered volcanic ashes in Palaeocene and Eocene sediments of the Eureka Sound Group (Ellesmere Island, Nunavut, Arctic Canada). Zeitschrift Dtsch. Gesellschaft Geowissenschaften 164, 131–147. doi: 10.1127/1860-1804/2013/0004

CrossRef Full Text | Google Scholar

Roest, W. R., and Srivastava, S. P. (1989). Sea-floor spreading in the Labrador Sea: a new reconstruction. Geology 17, 1000–1003.

Google Scholar

Røhr, T. S. (2009). Sedimentary Provenance Analysis of Lower Cretaceous Sedimentary Successions in The Arctic; Constraints From Detrital Zircon Data. Ph.D. thesis, University of Oslo.

Røhr, T. S., Andersen, T., and Dypvik, H. (2008). Provenance of lower Cretaceous sediments in the Wandel Sea Basin, North Greenland. J. Geol. Soc. Lond. 165, 755–767. doi: 10.1144/0016-76492007-102

CrossRef Full Text | Google Scholar

Rollins, M. B., and Pool, D. L. (1968). Measurement of exchangeable cations in bentonites. Clays Clay Miner. 16, 165–172. doi: 10.1346/CCMN.1968.0160207

CrossRef Full Text | Google Scholar

Saunders, A. D., Fitton, J. G., Kerr, A. C., Norry, M. J., and Kent, R. W. (1997). “The North Atlantic Igneous Province,” in Large Igneous Provinces: Continental, Oceanic, and Planetary Flood Volcanism, eds J. J. Mahoney and M. F. Coffin (Washington, DC: American Geophysical Union), 45–93.

Schlegel, A., Lisker, F., Dörr, N., Jochmann, M., Schubert, K., and Spiegel, C. (2013). Petrography and geochemistry of siliciclastic rocks from the Central Tertiary Basin of Svalbard – implications for provenance, tectonic setting and climate. Zeitschrift Dtsch. Gesellschaft Geowissenschaften 164, 173–186. doi: 10.1127/1860-1804/2013/0012

CrossRef Full Text | Google Scholar

Scotese, C. R. (2001). Atlas of Earth History, Vol. 1, Paleogeography. Arlington, TX: PALEOMAP Project.

Seton, M., Müller, R. D., Zahirovic, S., Gaina, C., Torsvik, T., Shephard, G., et al. (2012). Global continental and ocean basin reconstructions since 200 Ma. Earth Sci. Rev. 113, 212–270. doi: 10.1016/j.earscirev.2012.03.002

CrossRef Full Text | Google Scholar

Sircombe, K. N. (2004). AgeDisplay: an EXCEL workbook to evaluate and display univariate geochronological data using binned frequency histograms and probability density distributions. Comput. Geosci. 30, 21–31. doi: 10.1016/j.cageo.2003.09.006

CrossRef Full Text | Google Scholar

Smelror, M., Petrov, O. V., Larssen, G. B., and Werner, S. (2009). Atlas: Geological History of the Barents Sea. Trondheim: Geological Survey of Norway.

Google Scholar

Soloviev, A. V., and Miller, E. L. (2014). The U-Pb age dating of detrital zircons from Upper Jurassic-Lower Cretaceous deposits of Stolbovoy Island (New Siberian Islands). Stratigr. Geol. Correl. 22, 507–517. doi: 10.1134/S0869593814050086

CrossRef Full Text | Google Scholar

Soloviev, A. V., Zaionchek, A. V., Suprunenko, O. I., Brekke, H., Faleide, J. I., Rozhkova, D. V., et al. (2015). Evolution of the provenances of Triassic rocks in Franz Josef Land: U/Pb LA-ICP-MS dating of the detrital zircon from Well Severnaya. Lithol. Miner. Resour. 50, 102–116. doi: 10.1134/S0024490215020054

CrossRef Full Text | Google Scholar

Spielhagen, R. F., and Tripati, A. (2009). Evidence from Svalbard for near-freezing temperatures and climate oscillations in the Arctic during the Paleocene and Eocene. Palaeogeogr. Palaeoclimatol. Palaeoecol. 278, 48–56. doi: 10.1016/j.palaeo.2009.04.012

CrossRef Full Text | Google Scholar

Srivastava, S. P. (1985). Evolution of the Eurasian Basin and its implications to the motion of Greenland along Nares Strait. Tectonophysics 114, 29–53. doi: 10.1016/0040-1951(85)90006-X

CrossRef Full Text | Google Scholar

Steel, R. J., Dalland, A., Kalgraff, K., and Larsen, V. (1981). “The Central Tertiary basin of Spitsbergen: sedimentary development of a sheared margin basin,” in Geology of the North Atlantic Borderland: Canadian Society of Petroleum Geologists, Memoir 7, eds J. W. Kerr and A. J. Ferguson (Calgary: Canadian Society of Petroleum Geologists), 647–664.

Steel, R. J., Gjelberg, J., Helland-Hansen, W., Kleinspehn, K., Nottvedt, A., and Larsen, M. R. (1985). “The Tertiary strike-slip basins and orogenic belt of Spitsbergen,” in Strike-Slip Deformation, Basin Formation, and Sedimentation, Vol. 37, eds. K. T. Biddle and N. Christie-Blick (Tulsa: SEPM, Special Publication), 339–359.

Storey, M., Duncan, R. A., and Tegner, C. (2007). Timing and duration of volcanism in the North Atlantic Igneous Province: implications for geodynamics and links to the Iceland hotspot. Chem. Geol. 241, 264–281. doi: 10.1016/j.chemgeo.2007.01.016

CrossRef Full Text | Google Scholar

Storey, M., Duncan, R. A., Pedersen, A. K., Larsen, L. M., and Larsen, H. C. (1998). 40Ar/39Ar geochronology of the West Greenland Tertiary volcanic province. Earth Planet. Sci. Lett. 160, 569–586. doi: 10.1016/S0012-821X(98)00112-5

CrossRef Full Text | Google Scholar

Šucha, V., Kraus, I., Gerthofferová, H., Peteš, J., and Sereková, M. (1993). Smectite to Illite Conversion in Bentonites and Shales of the East Slovak Basin. Clay Miner. 28, 243–253. doi: 10.1180/claymin.1993.028.2.06

CrossRef Full Text | Google Scholar

Sun, S., and McDonough, W. F. (1989). Chemical and isotopic systematics of oceanic basalts: implications for mantle composition and processes. Geol. Soc. Lond. Spec. Publ. 42, 313–345. doi: 10.1144/GSL.SP.1989.042.01.19

CrossRef Full Text | Google Scholar

Taboada, T., Martínez Cortizas, A., García, C., and García-Rodeja, E. (2006). Particle-size fractionation of titanium and zirconium during weathering and pedogenesis of granitic rocks in NW Spain. Geoderma 131, 218–236. doi: 10.1016/j.geoderma.2005.03.025

CrossRef Full Text | Google Scholar

Talwani, M., and Eldholm, O. (1977). Evolution of the Norwegian-Greenland Sea. Bull. Geol. Soc. Am. 88, 969–999.

Google Scholar

Tarduno, J. A. (1998). “The high Arctic large igneous province,” in Abstract, Third International Conference on Arctic Margins (Celle: Federal Institute of Geosciences and Natural Resources).

Taylor, S. R., and McLennan, S. M. (1985). The Continental Crust: Its Composition and Evolution. Oxford: Blackwell.

Google Scholar

Tegner, C., Duncan, R. A., Bernstein, S., Brooks, C. K., Bird, D. K., and Storey, M. (1998). 40Ar-39-Ar geochronology of Tertiary mafic intrusions along the East Greenland rifted margin: relation to flood basalts and the Iceland hotspot track. Earth Planet. Sci. Lett. 156, 75–88. doi: 10.1016/S0012-821X(97)00206-9

CrossRef Full Text | Google Scholar

Tegner, C., Storey, M., Holm, P. M., Thorarinsson, S. B., Zhao, X., Lo, C.-H., et al. (2011). Magmatism and eurekan deformation in the high arctic large igneous Province: 40Ar-39Ar age of Kap Washington Group volcanics, North Greenland. Earth Planet. Sci. Lett. 303, 203–214. doi: 10.1016/j.epsl.2010.12.047

CrossRef Full Text | Google Scholar

Tessensohn, F., and Piepjohn, K. (2000). Eocene compressive deformation in Arctic Canada, North Greenland and Svalbard and its plate tectonic causes. Polarforschung 68, 121–124. doi: 10013/epic.29798.d001

CrossRef Full Text | Google Scholar

Tessensohn, F., Henjes-Kunst, F., and Krumm, S. (2001). “K/Ar Dating Attempts on Rocks from the West Spitsbergen Fold-and-Thrust Belt and the Central Basin,” in Intra-Continental Fold Belts CASE 1: West Spitsbergen, ed F. Tessensohn (Stuttgart: E. Schweizerbart'sche Verlagsbuchhandlung), 719–728.

Google Scholar

Thompson, B., Jakobsson, M., Nilsson, J., Nycander, J., and Döös, K. (2012). A model study of the first ventilated regime of the Arctic Ocean during the early Miocene. Polar Res. 31, 1–19. doi: 10.3402/polar.v31i0.10859

CrossRef Full Text | Google Scholar

Thompson, R. N. (1975). Palaeocene ignimbrite from Ubekendt Ejland, west Greenland. Lithos 8, 9–14. doi: 10.1016/0024-4937(75)90026-2

CrossRef Full Text | Google Scholar

Thompson, R. N. (1982). Magmatism of the British Tertiary Volcanic Province. Scottish J. Geol. 18, 49–107. doi: 10.1144/sjg18010049

CrossRef Full Text | Google Scholar

Thorarinsson, S. B., Holm, P. M., Duprat, H., and Tegner, C. (2011a). Silicic magmatism associated with Late Cretaceous rifting in the Arctic Basin–petrogenesis of the Kap Kane sequence, the Kap Washington Group volcanics, North Greenland. Lithos 125, 65–85. doi: 10.1016/j.lithos.2011.01.013

CrossRef Full Text | Google Scholar

Thorarinsson, S. B., Holm, P. M., Tappe, S., Heaman, L. M., and Tegner, C. (2011b). Late Cretaceous-Palaeocene continental rifting in the High Arctic: U-Pb geochronology of the Kap Washington Group volcanic sequence, North Greenland. J. Geol. Soc. London. 168, 1093–1106. doi: 10.1144/0016-76492011-018

CrossRef Full Text | Google Scholar

Torsvik, T. H., Carlos, D., Mosar, J., Cocks, L. R. M., and Malme, T. N. (2002). “Global reconstructions and North Atlantic paleogeography 440 Ma to Recent,” in BATLAS - Mid Norway Plate Reconstruction Atlas with Global and Atlantic Perspectives, ed E. A. Eide (Trondheim: Geological Survey of Norway), 18–39.

Tripati, A. K., Eagle, R. A., Morton, A., Dowdeswell, J. A., Atkinson, K. L., Bahé, Y., et al. (2008). Evidence for glaciation in the Northern Hemisphere back to 44 Ma from ice-rafted debris in the Greenland Sea. Earth Planet. Sci. Lett. 265, 112–122. doi: 10.1016/j.epsl.2007.09.045

CrossRef Full Text | Google Scholar

Tsikalas, F., Eldholm, O., and Faleide, J. I. (2002). Early Eocene sea floor spreading and continent-ocean boundary between Jan Mayen and Senja fracture zones in the Norwegian-Greenland Sea. Mar. Geophys. Res. 23, 247–270. doi: 10.1023/A:1023621228605

CrossRef Full Text | Google Scholar

Uroza, C. A., and Steel, R. J. (2008). A highstand shelf-margin delta system from the Eocene of West Spitsbergen, Norway. Sediment. Geol. 203, 229–245. doi: 10.1016/j.sedgeo.2007.12.003

CrossRef Full Text | Google Scholar

von Gosen, W., and Piepjohn, K. (2001). “Thrust Tectonics North of Van Keulenfjorden,” in Intra-Continental Fold Belts. CASE 1: West Spitsbergen, Geologisches Jahrbuch (Polar Issue No. 7), ed F. Tessensohn (Stuttgart: E. Schweizerbart'sche Verlagsbuchhandlung), 247–272.

Vonderbank, K. (1970). Geologie und Fauna der tertiären Ablagerungen Zentral-Spitzbergens. (Tromsø: Norsk Polarinstitutt), 153.

Wilson, M. (1989). Igneous Petrogenesis. London: Chapman & Hall.

Google Scholar

Winchester, J., and Floyd, P. (1977). Geochemical discrimination of different magma series and their differentiation products using immobile elements. Chem. Geol. 20, 325–343. doi: 10.1016/0009-2541(77)90057-2

CrossRef Full Text | Google Scholar

Worsley, D. (1986). Evolution of an Arctic Archipelago: The Geological History of Svalbard. Stavanger: Den norske stats oljeselskap a.s.

Keywords: Paleogene, Svalbard, Central Tertiary Basin, Basilika formation, bentonite, zircon provenance, High Arctic Large Igneous Province, North Atlantic Large Igneous Province

Citation: Elling FJ, Spiegel C, Estrada S, Davis DW, Reinhardt L, Henjes-Kunst F, Allroggen N, Dohrmann R, Piepjohn K and Lisker F (2016) Origin of Bentonites and Detrital Zircons of the Paleocene Basilika Formation, Svalbard. Front. Earth Sci. 4:73. doi: 10.3389/feart.2016.00073

Received: 30 March 2016; Accepted: 22 June 2016;
Published: 07 July 2016.

Edited by:

Craig Lundstrom, University of Illinois, USA

Reviewed by:

Lotte Melchior Larsen, Geological Survey of Denmark and Greenland, Denmark
Fernando Corfu, University of Oslo, Norway

Copyright © 2016 Elling, Spiegel, Estrada, Davis, Reinhardt, Henjes-Kunst, Allroggen, Dohrmann, Piepjohn and Lisker. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) or licensor are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.

*Correspondence: Felix J. Elling, felling@uni-bremen.de
Cornelia Spiegel, cornelia.spiegel@uni-bremen.de

Present Address: Felix J. Elling, Department of Earth and Planetary Sciences, Harvard University, Cambridge, MA, USA;
Niklas Allroggen, Institute of Earth and Environmental Science, University of Potsdam, Potsdam, Germany