ISSN 00244902, Lithology and Mineral Resources, 2015, Vol. 50, No. 2, pp. 102–116. © Pleiades Publishing, Inc., 2015. Original Russian Text © A.V. Soloviev, A.V. Zaionchek, O.I. Suprunenko, H. Brekke, J.I. Faleide, D.V. Rozhkova, A.I. Khisamutdinova, N.M. Stolbov, J.K. Hourigan, 2015, published in Litologiya i Poleznye Iskopaemye, 2015, No. 2, pp. 113–128.

Evolution of the Provenances of Triassic Rocks in : U/Pb LAICPMS Dating of the Detrital Zircon from Well Severnaya A. V. Solovieva, f, A. V. Zaioncheka, b, O. I. Suprunenkob, H. Brekkec, J. I. Faleided, D. V. Rozhkovaa, A. I. Khisamutdinovaa, N. M. Stolbovb, and J. K. Hourigane aGeological Institute, Russian Academy of Sciences, Pyzhevskii per. 7, Moscow, 119017 email: fission[email protected] bAllRussia Research Institute of Geology and Mineral Resources of the World Ocean, Angliiskii pr. 1, St. Petersburg, 190121 Russia cNorwegian Petroleum Directorate, Stavanger, Norway dUniversity of Oslo, Oslo, Norway eDepartment of Earth and Planetary Sciences, University of California, Santa Cruz, 1156 High Street, Santa Cruz, California, 95064, U.S.A. fRosgeologiya OJSC, ul. Khersonskaya 43/3, Moscow, 117246 Russia Received April 8, 2013

Abstract—Morphological analysis and U/Pb LAICPMS dating were carried out for detrital zircon (400 age determinations) from four core samples of Triassic rocks recovered by Well Severnaya (Graham Bell Island, Franz Josef Land Archipelago). It is shown that source areas were mainly composed of peraluminous gran ites. U/Pb LAICPMS zircon data were used to decipher the provenance evolution in the northern region. The main source of clastic material in the North Barents sedimentary basin in the Middle–Late Triassic was the Uralian fold belt, with lesser contribution from the (), Timanides, Taimyr, and rocks related to the Siberian plume. The clastic material was mainly transported from the south and southeast. From the beginning of the Middle to the terminal Late Triassic, influence of the Neoproterozoic sources systematically decreased, whereas contribution of Caledonian sources increased. DOI: 10.1134/S0024490215020054

INTRODUCTION tion of eroded complexes. In this work, the age, typo morphism, and the inner structure of detrital zircon The Franz Josef Archipelago is one of the key are studied to decipher the provenances and regional objects for reconstructing the history of the Triassic paleogeographic setting. sedimentation in the North Barents Sea region (Fig. 1). This study has a great scientific and applied signifi cance in relation with the presence of considerable TRIASSIC ROCKS hydrocarbon reserves in the Barents Sea. Reconstruc OF THE BARENTS SEA REGION tion of the age and composition of the provenance of clastic material for the Arctic Triassic rocks is an The study of the Arctic shelf has recently received urgent problem hotly debated during the last decade great attention. Mesozoic rocks within the Barents Sea (Miller et al., 2006; Pease et al., 2007; Petrov, 2010; Region have been studied sufficiently well from para Bue et al., 2011; Omma et al., 2012; Miller et al., metric and marine drilling data (Gramberg et al., 2013; Bue and Andersen, 2013). Singlegrain dating 1985; Bro et al., 1989). The Triassic terrestrial rocks with precision geochronological methods offers new were studied onland in the Svalbard Archipelago (Pch opportunities for studying terrigenous rocks. Zircon is elina, 1985, Mørk, 1999), Medvezhii and Nadezhda widespread in detrital rocks, being resistant to weath Islands (Pchelina, 1985), western Novaya Zemlya ering and decomposition. Individual grains of detrital Archipelago (Ustritskii, 1981), as well as in the para zircon are dated by U/Pb LAICPMS (Gehrels, metric boreholes on the Franz Josef Land (Preo 2011; and others). Their morphology bears important brazhenskaya et al., 1985). Triassic rocks of the Nor information on provenances (Zircon, 2003), while wegian Barents Sea were studied in marine boreholes typomorphism (Pupin, 1980; Belousova et al., 2006) (Bugge and Fanavoll, 1995; Mørk, 1999). Thickness of provides insight into physicochemical conditions the Triassic rocks varies from 690 to over 3800 m (temperature, pressure, agpaitic index) of the forma (Basov et al., 2009). Within the Barents Sea region, the

102 EVOLUTION OF THE PROVENANCES OF TRIASSIC ROCKS IN FRANZ JOSEF LAND 103

180°

e Amerasian g Anabar id Shield R T Basin v Canadian e p a le e im e ge Shield d De y n v id r e o ko v R r Siberian M r o o – a s Northern g a M o e traps h n n n lp o a Land A m i 270° o s 90° L a n r si Franz u a West E B Josef Siberian C Land N Basin o v a Z y Baffin e a Bay m ly d a P n o o r lar la o n d n g U e l e e r e ie g n a r o l h r o G S ro O g Svalbard Barents en Labrador n ia Sea n n Sea o e Timan orogen d g le o a r C O n ia n Baltic o d Shield le a C

0° 1 4 7 10 13 2 5 8 11 C 14 3 6 9 12

Fig. 1. Tectonic scheme of the West Arctic region (Omma et al., 2011). (1) Greenland glaciers; (2) land; (3–5) sea depth, m: (3) 0–400, (4) 400–3500, (5) >3500; (6) tectonic boundaries; (7) inferred tectonic boundaries; (8) fields of basalts and volcanic belts (≤252 Ma); (9) Precambrian shields; (10–13) orogens: Late Paleozoic–Early Mesozoic Hercynian (Uralian); (11) Early Paleo zoic Ellesmirian; (12) Early Paleozoic Caledonian; (13) Neoproterozoic–Cambrian Timan; (14) position of Well Severnaya in Graham Bell Island, Franz Josef Land Archipelago.

Triassic rocks are represented by terrigenous rocks of matite gabbro, and olivine gabbrodolerites (Gramberg different facies with carbonate interbeds and nodules. et al., 1985). The presence of sandstones at different stratigraphic levels in the borehole section (Fig. 2) In the 1970s, islands of Franz Josef Land were allowed us to collect samples for the heavy fraction studied by three parametric boreholes: Nagurskaya, analysis and the detailed study of detrital zircon grains. Severnaya, and Hayes (Gramberg et al., 1985). Well Core samples were taken from different depths and Severnaya reached a depth of 3523 m in Graham Bell stratigraphic levels (Fig. 2). Island of the Franz Josef Archipelago, but did not leave Triassic rocks (Preobrazhenskaya et al., 1985; Sample C2688 was taken from the Middle Triassic Dypvik et al., 1998). Well Severnaya recovered the (upper Anisian) sandstones at a depth of 2688 m; sam Upper and Middle Triassic rocks (Figs. 1, 2). The ple C2073 (sandstone) was taken from Middle Triassic Upper Triassic sequence comprises the Norian and (upper Ladinian) detrital rocks at a depth of 2073 m; Raethian clayey–aleuritic sediments and Carnian sample C1040 was collected from Late Triassic (upper mainly sandy—aleuritic sediments intercalated with Carnian) psammites at a depth of 1040 m (Preo coaly rocks and lenses of bituminous coal (Gramberg brazhenskaya et al., 1985; Dypvik et al., 1998); and et al., 1985). The Middle Triassic sequence is domi sample C633 (aleurosandstones) with the inferred nated by Ladinian and Anisian alueritic–clayey sedi Upper Triassic (upper Norian) age was taken at a ments. The borehole recovered six intrusive bodies depth of 633 m. from 5 to 87 m thick (Fig. 2). The igneous rocks are The samples are medium to coarsegrained represented by dolerites, microdolerites, micropeg polymictic sandstones corresponding to feldspar–

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015 104 SOLOVIEV et al. Stage Series System Age, Ma Depth, m Lithology 500

C633 Norian

~228 915 1000 C1040 Upper

1500 Carnian

M

Triassic 2000 ~235 2012 С2073 1 2 3

Ladinian 4 5 2500 6 ~242 2530 7 8 M С2688 9 10 11 Middle 12 3000 13 14 Anisian 15 16 17 M 18 19 3500 С1040 20 Borehole bottom 3525

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015 EVOLUTION OF THE PROVENANCES OF TRIASSIC ROCKS IN FRANZ JOSEF LAND 105

Fig. 2. Fragment of Well Severnaya section, Franz Josef Land Archipelago. Modified after (Preobrazhenskaya et al., 1985; Dypvik et al., 1998). (1–4) Rocks: (1) argillites, (2) sandstones, (3) aleurolites, (4) igneous; (5, 6) matrix: (5) calcitic, (6) dolomitic; (7– 12) structures: (7) laminated, (8) crossbedded, (9) hummocky crossbedded; (10) bioturbation traces; (11) loading structure, (12) ripple marks; (13) fauna, (14) plant detritus; (15) plant remains; (16, 17) nodules: (16) pyrite, (17) siderite; (18) mica; (19) coal; (20) number of samples collected for the analysis of detrital zircon. quartz (sample C2688) and quartz–feldspar and devitrified volcanic glass. The matrix is porous and graywackes (sample C1040). They are made up of contoured and shows a patchy distribution in the rock. quartz (30–40%), feldspars (25–35%), rock frag Thinbedded aleurosandstone (sample C633) is ments (15–40%), mica (5%), organic matter (5%), made up of quartz (85%), feldspars (7%), altered rock and accessory minerals. Quartz forms both rounded fragments (5%), and muscovite (3%). Quartz is repre and irregularly shaped grains with corroded bound sented by weakly rounded or less common rounded aries. The prevailing monocrystalline quartz has a monocrystalline grains with straight extinction. The straight, more rarely undulose extinction, while the grains are practically devoid of gas–liquid inclusions less common poorly rounded polycrystalline quartz and fractures. Polycrystalline quartz is absent. Feld displays undulose and mosaic extinction. Feldspars are spars are mainly represented by tabular (95%) plagioclase and microcline. Their crystals have a tabu untwinned unaltered plagioclase and rare micrcoline. lar, rarely equant, habit. There are also twinned crys Weakly deformed muscovite flakes with high interfer tals and grains with clearly expressed microcline cross ence color and clear cleavage fractures are often ori hatching, as well as scarce intergrowths of feldspar and ented parallel to bedding. Accessory minerals are rep quartz. Rock fragments are represented by quartzites resented by rare zircon grains. Rock fragments pre with typomorphic microcrystalline appearance, fel sumably represent volcanic glass. Matrix occupies sitic volcanic rocks, and devitrified glass. The volcanic 40% of polished thin section area and consists of rocks and glass usually experienced secondary alter clayey–carbonate aggregate, (locally, secondary chlo ation, being replaced by finescale clayey aggregate. rite) with uneven patchy distribution of organic mate Biotite and muscovite occur as weakly bent altered rial. Bedding is caused by uneven banded distribution flakes up to 0.7 mm long. They are localized in the of clay material. Aleurosandstone is cemented by interstices, enveloping quartz and feldspar. Accessory mixed matrix: continuous uneven, open porous, and locally, basal. minerals are represented by rounded and prismatic zircon. Matrix accounts for 10–20% of polished thin section area and has a mixed composition. Carbonate METHODS AND RESULTS replacement matrix is developed after plagioclase. In general, sandstones have a clayey–carbonate matrix Heavy Fraction Minerals with locally developed zones consisting of small frag Heavy fraction minerals were extracted using con ments of plagioclase, quartz, clay minerals, carbonate, ventional technique at the Laboratory of Mineralogi

C633 (T3nor)

C782 (T3nor)

C9301–984.4 (T3car)

C1040 (T3car)

C1428 (T3car)

C2073 (T2lad)

C2688 (T2an)

0 102030405060708090100%

123

Fig. 3. Distribution of heavy fraction minerals in sandstones from Well Severnaya. Indicator minerals of source areas: (1) sialic rocks (zircon, apatite, rutile, and tourmaline); (2) mafic rocks (spinel, ilmenite, leucoxene); (3) cosmopolitan minerals (anatase, brookite, garnet, monazite, magnetite, sulfides, sphalerite, staurolite, amphibole, chlorite, mica, carbonate, iron hydroxides, biotite).

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015

106 SOLOVIEV et al.

Biotite

Iron hydroxides Iron

Carbonate

Mica

Chlorite

Amphibole

Staurolite

Sphalerite

Sulfides

Magnetite

the heavy fraction Ilmenite

Tourmaline

Spinel Monazite

Mineral content (%) in

Garnet

Leucoxene Brookite

from Well Severnaya, Franz Josef Land Archipelago Severnaya, Well from

Anatase Rutile

depth. Dash denotes mineral was not found. depth. Dash denotes mineral was

Apatite

Zircon

Heavy fraction output (%) output fraction Heavy

Heavy fraction weight (mg) weight fraction Heavy Sample weight (g) weight Sample 800 2051.0 0.26 0.22 0.26 0.10 0.01 0.02 0.75 0.02 – 0.07 0.05 – – 0.01 – – 0.01 – – – 98.49

Analysis of heavy fraction minerals in sandstones Sample no.* Sample C633 830 10581.1 1.27C782 0.95 0.06 1485 0.63 398.1 0.01 0.03C930.1– 0.07 13.69941.4 2.99 2.41 12.06 0.83 0.38 – –C1040 1.46 18.34 0.37 18.46 670 3.05 – 1206.5 0.18 0.18 19.84 2.55C1428 3.77 3.58 9.04 – 2.86 570 1.48 – 1012.5 0.39 0.03 0.18 –C2073 0.17 – 8.26 10.03 13.73 1500 – 7.63 5.37 4988.3 – 0.86 0.33 – – – 0.33C2688 – 4.23 83.89 0.72 13.04 0.97 550 2.58 – 0.46 5.19 1631.6 0.01 – – 0.30 – – –* 6.74 Sample number corresponds to the sampling – 4.59 1.84 – 1.35 2.04 0.12 9.07 0.35 0.01 – – – – 3.68 17.34 2.01 – – 24.33 0.25 0.10 0.37 – – 1.52 – 4.24 1.36 – – – – – 3.75 – – 0.04 – 0.92 67.55 – 1.21 – 45.43 – – – 0.16 88.21 – – 15.44 0.28 4.01 – – 14.77 Table 1. Table

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015 EVOLUTION OF THE PROVENANCES OF TRIASSIC ROCKS IN FRANZ JOSEF LAND 107

Table 2. Content (%) of zircons of different morphological types (Pupin, 1980) in the core from Well Severnaya (Franz Jo sef Land Archipelago)

Sample Morphological type Age N no.* H L1 L3 L4 G1 I Q2 S6 S7 S9 S15 S19 S21 S22 S24 S25

C2688 T2 (upper 12.7 24.1 5.4 11.3 0.0 0.0 0.0 5.4 6.7 12.7 9.4 0.7 0.0 1.3 2.9 7.4 149 Anisian) C2073 T2 (upper 9.4 22.6 2.2 2.9 0.0 1.4 3.6 7.3 8.0 9.4 8.7 0.0 1.4 4.3 2.9 15.9 138 Ladinian) C1040 T3 (upper 17.1 25.0 7.8 9.4 0.0 0.0 0.0 3.1 0.0 25.0 6.3 1.6 0.0 3.1 0.0 1.6 64 Carnian) C633 T3 (upper 11.2 24.4 0.7 14.0 1.4 0.0 1.4 8.4 7.0 11.2 7.0 1.4 1.4 2.1 1.4 7.0 143 Norian) * Sample number corresponds to the sampling depth in a well. N is the number of calculated grains. Designations of morphological types correspond to united fields: H = H + Q1, L1 = L1 + L2 + S1 + S2, L3 = L3 + S3, L4 = L4 + L5+S4 + S5, G1 = G1 + P1, I = I + R1, Q2 = Q2 + Q3, S6 = S6 + S11, S7 = S7 + S8 + S12 + S13, S9 = S9 + S10 + S14, S15 = S15 + P3 + S20 + P4, S19 = S19, S21 = S21 + J1, S22 = S22 + S23 + J2 + J3, S24 = S24 + J4, S25 = S25 + P5 + J5 + D. cal and Track Analysis of the Geological Institute, dral particles account for 20–30% of all zircon grains Russian Academy of Sciences. The examination of (Table 2, Fig. 4a). heavy fraction revealed a wide range of minerals (Table 1, Sample C2073 contains colorless, pale yellow, and Fig. 3). The minerals are grouped into indicators of pale pink zircon. Grains of volcanic origin (2 to 3%) sialic rocks (zircon, apatite, rutile, and tourmaline); have elongation coefficient of 3–5. They are colorless mafic rocks (spinel, ilmenite, leucoxene); and cosmo and pale yellow, without visible inclusions. There are politans (anatase, brookite, garnet, monazite, magne also scarce transparent zircons with vague cores. Some tite, sulfides, sphalerite, staurolite, amphibole, chlo crystals contain inclusions of black, sometimes acicu rite, mica, carbonate, iron hydroxides, and biotite). lar, mineral (probably rutile). Euhedral grains account The obtained data did not allow us to reveal a clear for 10–15% (Table 2). trend or the predominance of a definite provenance. Sample C1040 contains a few zircon grains. There Samples C782, C1428, and C2688 contain significant fore, only a limited number of grains were used for cal amounts of minerals that are typical of felsic and basic culation (Table 2). rocks (in equal proportions). Some samples (C633, Sample C633 contains transparent zircon, with the C 930941.4, C1040) comprise a large amount of sec predominance of pale yellow, yellow, and pale orange ondary minerals: siderite (C633) and iron hydroxide grains. Colorless zircon is rare. The crystals host dust (C930—941.4, C1040), which indicate a high degree inclusions of black mineral. Euhedral grains account of rock transformation. for 20–25% (Table 2, Fig. 4b). Crystallomorphological analysis showed that all Morphology of Detrital Zircons samples contain zircon of mainly H, L1, L4, S6, S7, S9, S15, and S25 types. According to the diagram Only euhedral zircons (10–30% of all zircons) were (Belousova et al., 2006), H and L1 zircons are typical morphologically analyzed and calculated. Calcula of Stype peraluminous granites; L4, of hybrid tions were carried out using a Meiji ZOOM RZB monzonites and alkaline granites; S6 and S7, of calc series stereomicroscope, which provides a highreso alkaline granites; S9, of contaminated subalkaline and lution sharp image undistorted under magnification alkaline granites; S15, of Itype subalkaline and alka up to 300. For convenience in calculation, we modi line granites; and S25, of Itype alkaline and tholeiitic fied the zircon classification (Pupin, 1980). The dis granites. This analysis illustrates that zircons were tinguished groups included morphological types with derived from granitoids of different types. All samples similar structure without allowance for the elongation demonstrate the sharp predominance (32–42%) of coefficient. Each of the groups was termed according euhedral zircons typical of peraluminous granites (H to the left morphological type in the classification and L1). (Pupin, 1980) (Table 2, Fig. 4). Sample C2688 comprises colorless, light pink, and yellowish pink zircon. Some grains are “fused” and U/Pb Zircon Dating by Laser Ablation (LAICPMS) have corroded surface, but the majority of zircon are Analyses were carried out at the University of Cal characterized by even lustrous faces. Accumulations of ifornia Santa Cruz LAICPMS laboratory using an small inclusions observed in some grains impart gray Element XR highresolution magneticsector ICP ish color to the mineral. Individual crystals contain MS and a Photon Machines Analyte.H 193 nm eximer intergrowths of brownblack acicular rutile (?). Euhe laser equipped with a Helex 2volume laser ablation

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015 108 SOLOVIEV et al.

(a) А index ±50° 100 200 300 400 500 600 700 800 500°C B AB1 AB2 AB3 AB4 AB5 A C 550°C No prisms 100

H L1 L2 L3 L4 L5 G1 I 600°C 110 200

Q1 S1 S2 S3 S4 S5 P1 R1 ° 650 C 100 Ӷ 110 300

Q2 S6 S7 S8 S9 S10 P2 R2 700°C 100 < 110 400

Q3 S11 S12 S13 S14 S15 P3 R3 index Prisms 750°C 100 = 110 500 T

Q4 S16 S17 S18 S19 S20 P4 R4 800°C 100 > 110 600

Q5 S21 S22 S23 S24 S25 P5 R5 ° 850 C 100 ӷ 110 700

E J1 J2 J3 J4 J5 D F 0.1–1% ° 1.1–5% 900 C 100 800 5–10% >10% 211 101 Ӷ 211 101 < 211 101 = 211 101 > 211 101 ӷ 211 101 301 Pyramids (b) А index ±50° 100 200 300 400 500 600 700 800 500°C B AB1 AB2 AB3 AB4 AB5 A C 550°C No prisms 100

H L1 L2 L3 L4 L5 G1 I 600°C 110 200

Q1 S1 S2 S3 S4 S5 P1 R1 ° 650 C 100 Ӷ 110 300

Q2 S6 S7 S8 S9 S10 P2 R2 700°C 100 < 110 400

Q3 S11 S12 S13 S14 S15 P3 R3 index Prisms 750°C 100 = 110 500 T

Q4 S16 S17 S18 S19 S20 P4 R4 800°C 100 > 110 600

Q5 S21 S22 S23 S24 S25 P5 R5 ° 850 C 100 ӷ 110 700

E J1 J2 J3 J4 J5 D F 0.1–1% 900°C 800 1.1–5% 100 5–10% >10% 211 101 Ӷ 211 101 < 211 101 = 211 101 > 211 101 ӷ 211 101 301 Pyramids

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015 EVOLUTION OF THE PROVENANCES OF TRIASSIC ROCKS IN FRANZ JOSEF LAND 109 cell. Ablated aerosol was transported through 4mm limit of detection of three times the standard devia inner Teflon tubing. The ALTEX laser is energy stabi tions. For this reason, the 204Pb correction was lized at 4.5 mJ. The energy density control was pro replaced by the 207corrected 206Pb/238Pb age. vided by a user settable attenuator. Grains of detrital zircon extracted from the core of The grains of detrital zircon were mounted in rows Well Severnaya were dated by U/Pb LAICPMS. One on doublesided sticky tape using a mask cut from the hundred grains were dated from each sample. The tape backing film. Zircon standards SL2 (563 Ma; concordia (Wetherill, 1956) and Tera Wasserburg (Tera Gehrels et al., 2008) and Plesovice (337 Ma; Slama and Wasserburg, 1972) diagrams were plotted using et al., 2008) were mounted at the center of the mount. ISOPLOT 3.0 (Ludwig, 2003) (Fig. 5). Calculations Then, the grains were potted in a ring form using were made only for concordant grains (Figs. 5, 6). Zir Struers Epofix epoxy resin. The solidified mount was con in all samples shows a wide age range (Fig. 6). The cut off to the required size using a turning machine. The mount surface with zircon grains was successively studied sandstones contain zircons of Mesozoic, Pale polished with 1500 grit sandpaper, 9 and 3 µm Struers ozoic, and Precambrian ages in different proportions polishing compounds on a LaboPol lap wheel. (Fig. 6). Cathodoluminescence images were obtained at the Grains with an age of 276.2 ± 1.4 Ma (±2σ, seven Microanalytical Center of the Stanford University grains) are distinctly distinguished in sandstone (sam (http://shrimprg.stanford.edu) using a JEOL JSM ple C2688, upper Anisian). This sample also contains 5600 scanning electron microscope with cathodolu zircon of the following age intervals: 280–300 and minescence detector. 320–360 Ma with clearly expressed peak at 343 Ma; A series of four primary SL2 (Gehrels et al., 2008) 590–790 Ma and 590–790 Ma with main peak at 632 and secondary Plesovice (Slama et al., 2008) standards Ma (Fig. 6). No zircons older than 800 Ma were found were analyzed at the beginning and end of each sec in this sample. cion. Primary standard was analyzed after every fifth analysis of grains of unknown age and were paired with Sample C2073 (upper Ladinian) contains a great secondary standard after every tenth analysis. Accord amount (48) of discordant grains. The concordant ing to the measurement protocol, 15 secondary stan ages of zircon are distributed over intervals (Ma): 240– dard zircons were analyzed per 100 analyses to moni 250, 290–360, and 440–690. Zircon grains older than tor the quality and accuracy of measurements. The 700 Ma are rare. Insignificant peaks are noted at 1424 obtained data were reduced using the Iolite addons and 1540 Ma. for Igor Pro (Paton et al., 2010). It was taken that the Sandstone (sample C1040) contains zircon with an exponential detrending algorithm based on the down age of 218.8 ± 6.4 Ma (±2σ, three grains), which is hole fractionation of standards is more reliable than slightly younger than the sedimentation age deter the linear regression technique, “ratioofmeans” or mined by biostratigraphic methods (Upper Triassic, “meanofratios” data reduction methodologies. In upper Carnian) (Preobrazhenskaya et al., 1985; Dyp particular, we favor the detrending approach, because vik et al., 1998). This may be the reason for the revision unknowns that exhibit different fractionation behavior of age of the given stratigraphic interval. The obtained support a temporal trend after downhole correction, data suggest that sedimentation in the Late Triassic which leads to the higher standard deviation when sig (Norian) was accompanied by volcanism (and/or nal is averaged. Thus, the accuracy is estimated as the magmatism) in the surrounding structures. Zircon ages difference between the ablation behavior of the stan are grouped into following age intervals: 220–245 Ma dards and grains of unknown age. with clearly expressed peak at 233 Ma; 250–490 Ma Synchronization and the reproducible sample with peaks at 259, 309, 345, 400, and 460 Ma (Fig. 6). washout of the Helex2 allow the automatic integra Zircon older than 500 Ma does not define statistically tion based on fixed time intervals without modifica significant peaks, except for the peak at 791 Ma. tions for 90% of typical samples. Integration regions are resized if grain was burned through by laser, which A significant amount of zircon found in sample is expressed in a sharp decrease of signal during laser C633 has the Norian age, which is presumably close to operation, or spikes of 204Pb are observed among the the formation time of sandstones. The following age background values. Total 204Pb backgrounds (Pb + intervals are distinguished: 220–235, 270–280, and Hg) usually account for ~300 ± 10 counts per second. 310–315 Ma. There is a clearly expressed peak at 490– Other than 204Pb peaks related to the inclusions or high 540 Na with maximum at 511 Ma (Fig. 6). Zircons U content (high damage degree?), the average back older than 600 Ma do not define the statistically signif ground signals are typically less than the established icant peaks, except for the peak at 1460–1530 Ma.

Fig. 4. Morphological classification of zircon crystals (Pupin, 1980). Shown is the content of detrital zircon of different morpho logical types in sandstone samples: (a) C2688, (b) C633 (Table 2). Index A is the Al/(Na + K) ratio controlling the development of zircon pyramids, index T shows the temperature affecting the development of zircon prism.

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015 110 SOLOVIEV et al. . (1) Concordant σ 2 ± 3400 pse size is given in pse size is given U Pb 235 206 20 40 U/ Pb/ 238 207 400 3000 10 2600 2200 1200 030 0 1020304050

0.1 0.6 0.4 0.3 0.2 0.4 0.2

U Pb Pb/ (c) Pb/ (d)

238 206 206 207 1 2 900 U Pb 235 206 concordia, (b) Tera—Wasserburg); C633: (c) concordia, (d) TeraWasserburg. Error elli C633: (c) concordia, (d) TeraWasserburg. concordia, (b) Tera—Wasserburg); Pb/ 400 U/ 700 207 238 12 600 500 800 300 1000 1200 1400 0 0.4 0.8 1.2 1.6 2.0 4 8 16 20 24 28

(a) (b)

0.16 0.10 0.18 0.10 0.14 0.14 0.12 0.12 0.08 0.06 0.04 0.02 0.08 0.06 0.04 U Pb/ Pb Pb/

238 206 206 207 Isotope diagrams for samples. C2688: (a) determinations, (2) discordant determinations. Fig. 5.

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015 EVOLUTION OF THE PROVENANCES OF TRIASSIC ROCKS IN FRANZ JOSEF LAND 111 = 43 = 80 = 96 = 75 N N N N ), ), ), ), С633 С1040 С2073 С2688 791 0.54–1 Sample Sample Sample Sample 725 upper Norian upper Anisian upper Carnian Neoproterozoic upper Ladinian ( ( ( 3 ( 2 3 2 T T T 5% 12% T 38% 33% 632 598 600 594 545 511 (b) Age, Ma 460 4% 10% dated grains. 26% 17% 0.39–0.5 400 392 Caledonides 343 345 37% 309 71% 38% 312 274 285 302 58% 245 259 0.22–0.37 276 231 200 300 400 500 700 800 900 1000 233 in samples from Well Severnaya in coordin ates: (a) 0–3200 Ma, (b) 0–1000 Ma. N Severnaya Well in samples from 0100 e given age interval in the total number of age interval e given = 52 = 83 = 96 = 86 N N N N ), ), ), ), ), С633 С1040 С2073 С2688 Sample Sample Sample Sample upper Norian upper Anisian upper Carnian upper Ladinian ( ( ( 3 ( 2 3 2 T T T T 1.6–2.5 distribution diagrams for detrital zircon 6% 4% 0% 2% Paleoproterozoic rcents denote the number of grains th (a) Age, Ma 1424 7% 0% 11% 1–1.6 Mesoproterozoic 791 5% 1% 12% 38% 33% 725 0.54–1 632 Neoproterozoic 545 511 460 392 343 345 312 274 Normalized probability density (frequency) 302 309 245 276 0.22–0.37 233 231 Fig. 6. is the number of dated concordant values. Pe is the number of dated concordant values. 38% 26% 71% 17% 37% 10% 58% 4% 0 500 1000 1500 2000 2500 3000

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015 112 SOLOVIEV et al.

S9 L4 S9 306.7 ± 3.4 21346.421 ± 4.0 24 22 622.4 ± 5.4 23 H 623.3 ± 4.5 H 642.4 ± 3.6 S25 H 6 S9 609.0 ± 2.9 668.8 ± 4.2 L1 7 285.0 ± 1.7 8 4 S15 S25 9 295.7 ± 2.0 5 26 776.4 ± 6.2 704.5 ± 6.6 642.3 ± 4.2 11 322.7 ± 1.7 10 390.9 ± 2.1 3 12 275.4 ± 1.9 333.9 ± 2.0 1 826.0 ± 2.0 2 39 39 A µ 15 kV2 200 m

Fig. 7. Cathodoluminescence images of the detrital zircon from sample C2688. Circles show the concordant ages, numeral denotes the number of dated zircon. Age is given with error ±1σ. Morphological types of crystals are given after (Pupin, 1980).

Comparison of the Zircon Age and Morphology increases in the Norian (sample 633, 13%) (Fig. 6). Morphology of detrital zircon was also analyzed The Paleo and Mesoproterozoic zircons were pre using images obtained by cathodoluminescence sumably derived from the East European Craton (Bal detector mounted on a JEOL JSM 5600 scanning tica) (Patchett and Kuovo, 1986; Bogdanova et al., electron microscope (Fig. 7). There is no clear corre 2008; Bingem and Soll, 2009), although zircon of this lation between morphology and age of zircons. For age interval is also known in northern Laurentia (Hei instance, euhedral grains, which are dominant in the nriksen et al., 2000). Note that Baltica is a more pref studied samples and typical of peraluminous granites erable provenance, because zircons with ages of 1.48– (H and L1) (Belousova et al., 2006), have a wide age 1.64 Ga found in samples from Well Severnaya are range (Fig. 8). absent in Laurentia. The Grenvillian (1.14–0.9 Ga) provenances did not affect the Triassic sedimentation, because samples PROVENANCE EVOLUTION from Well Severnaya contain only three zircons of this AND PALEOGEOGRAPHIC age (Bogdanova et al., 2008; Lorenz et al., 2012). RECONSTRUCTIONS The Neoproterozoic (1.0–0.54 Ga) zircons were The studied samples are sharply dominated by delivered to sediments in significant amounts in the Paleozoic and Mesozoic zircons, with a significant Anisian (0.8–0.56 Ga) (38%) and Ladinian (0.84– amount of Neoproterozoic zircons, insignificant 0.54 Ga) (33%). They factually disappeared in the Meso and Neoproterozoic zircons, and practical Carnian (5%) and again appeared in the Norian absence of Archean zircons. (12%). Sources of the Neoproterozoic zircon are Samples from Well Severnaya (Franz Josef Land widespread in the surrounding structures of the Bar Archipelago) contain only two Archean grains (>2.5 Ga), ents Sea, along the eastern front of the Polar Urals, thus indicating that Archean provenances played no and in Novaya Zemlya, Scandinavia, and Svalbard role in the accumulation of Triassic rocks in this (Kuznetsov et al., 2010). Neoproterozoic magmatic region. rocks related to the Timan served as signifi Zircons of the Paleo and Mesoproterozoic (2.5– cant source of zircon of this age in the Barents Sea 1.0 Ga) age are absent in the Anisian sandstones (sam region (Larionov et al., 2004; Pease, 2011). Sources ple C2688). They appear in significant amount (15%) with an age of 630–615 Ma are known in the central only in the Ladinian rocks (sample C2073) (1.8–1.6 Taimyr (Pease and Vernikovsky, 2000). Vendian detri and 1.4–1.5 Ga). The role of these sources becomes tal zircons (650 Ma) were found in the northern weaker (3%) in the Carnian (sample 1040) and again Taimyr (Pease and Scott, 2009). Granitoids of this age

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015 EVOLUTION OF THE PROVENANCES OF TRIASSIC ROCKS IN FRANZ JOSEF LAND 113

7

6

5

4

3 Number of grains 2

1

0200400 600 800 1000 1200 1400 1600 Age, Ma

Fig. 8. Bar charts for the detrital zircon of morphological types H and L1 (Pupin, 1980) that are typical of peraluminous granites in samples from Well Severnaya (Franz Josef Land Archipelago). are also typical of the western Siberian Craton (Verni Brown et al., 2006; Pease, 2011). The youngest zircons kovsky et al., 2003). We believe that the main sources (250–220 Ma) were presumably derived from mag of the Neoproterozoic zircon in the studied samples matic and volcanic rocks that are related to the Sibe were the Polar Urals and, possibly, Novaya Zemlya and rian plume and known in Taimyr (Vernikovsky et al., Taimyr. 2003; Walderhaug et al., 2005) and Siberian Craton The amount of zircon related to the Caledonian (Reichow et al., 2009), as well as in boreholes in (500–390 Ma) stage systematically increases from the northern West (Saraev et al., 2009; Nikishin Anisian (400–390 Ma, 4%), Ladinian (500–440 Ma, et al., 2011). 10%), Carnian (480–390 Ma, 17%) to the Norian Results of the dating of detrital zircon from Well (500–390 Ma, 26%). Thus, the Caledonian com Severnaya provide insight into the evolution of prove plexes were gradually exhumed by the beginning of the nances for the northern part of the Barents Sea in the Middle Triassic to play a significant role during the Middle–Late Triassic. Late Triassic erosion. Zircons with age of 500–480 Ma The Middle Triassic (upper Anisian) clastic mate were presumably derived from eroded magmatic rocks rial was mainly delivered from the Hercynian struc that were formed at the final stage of the Timan Orog tures of the Polar Urals. These sources fed the basin eny (Gee et al., 2000; Kuznetsov et al., 2007) or during with zircons of 370–270 Ma. Sources of Neoprotero rifting of the Ordovician passive margin of the Urals zoic zircon (800–560 Ma), second in significance, are (Puchkov, 1997). Magmatic and metamorphic rocks inferred to be rocks of the eastern front of the Polar formed in the Caledonian time are known on the Sev Urals, Novaya Zemlya, and northern and central ernaya Zemlya Archipelago (490–410 Ma) (Lorenz Taimyr. Clastic material was delivered from the south et al., 2007) and Svalbard (470–410 Ma) (Myhre and southeast. et al., 2008; Petterson et al., 2010). By the end of the Middle Triassic (upper Ladinian), Zircon dated within 370–320 Ma forms the most the Hercynian (360–270 Ma) and Neoproterozoic significant peak in all samples: Anisian (370–270 Ma, (840–540 Ma) rocks remained the main zircon 58%), Ladinian (360–270 and 270–240 Ma, 37%), sources, but their contribution decreased. Erosion of Carnian (370–270 Ma and 270–220 Ma, 71%), and the PermoTriassic magmatic and volcanic rocks Norian (370–270 Ma and 270–220 Ma, 38%). Zircon (250–220 Ma) introduced a new source area. Transfer of the age interval from 370 to 300 Ma and, possibly, to from the Caledonian structures increased, and zircon 270 Ma is related to the Hercynian (Uralian) magma grains with age of 500–440 Ma were derived from both tism, the manifestations of which are known in the the south (Late Timanides, Polar Urals) and east (Sev Polar Urals and Taimyr (Zonenshain et al., 1990; ernaya Zemlya Archipelago). Transportation from the

LITHOLOGY AND MINERAL RESOURCES Vol. 50 No. 2 2015 114 SOLOVIEV et al. west (Svalbard Archipelago) is less probable. At the paper allowed us to significantly specify the prove end of the Middle Triassic, the Paleo and Mesoprot nances of Triassic rocks in the Barents Sea region erozoic rocks of the East European Craton (Baltica) (Pease et al., 2007; Petrov, 2010; Bue et al., 2011; Bue began to erode. and Nadersen, 2013). Thus, the U/Pb dating of detri The beginning of the Late Triassic (upper Carnian) tal zircon bears important information on prove is marked by increasing erosion of magmatic rocks nances and provides the correction of regional paleo related to the Siberian plume (250–220 Ma) and a geographic reconstructions. detrital supply from the Hercynian (370–270 Ma) and Caledonian (480–390 Ma) structures. Paleo Meso, and Neoproterozoic rocks were virtually not eroded. CONCLUSIONS The end of Triassic (upper Norian) was marked by (1) Morphological analysis of detrital zircon crys decrease in erosion of rocks with age of 250–220 Ma tals from four core samples of the Triassic rocks recov and 370–270 Ma (Hercynian sources) and increase in ered by Well Severnaya in the Franz Josef Land Archi the contribution of Caledonian (500–390 Ma) com pelago showed that the main source rocks were peralu plexes. Erosion of the Paleo, Meso, and Neoprot minous granites in association with calcalkaline, erozoic rocks was intensified. subalkaline, and alkaline granitoids. Thus, the main sources of clastic material in the (2) The LAICPMS U/Pb data on detrital zircons North Barents Sea sedimentary basin in the Middle— (400 age determinations) were used to decipher the Late Triassic were structures of the Uralian fold belt, evolution of provenance for the Barents Sea region in with a lesser contribution of the East European Cra the Middle—Late Triassic. At the beginning of the ton, Baltica, Timanides, Taimyr, and Siberian traps. Middle Triassic, the main sources of clastic material The material was presumably delivered mainly from were Hercynian structures of the Urals. Sources of the the south and southeast. The contribution of the Neoproterozoic zircon, second in significance, were Neoproterozoic sources systematically decreased, the complexes of the Polar Urals. It could also be while the role of the Caledonian sources increased transported from Novaya Zemlya and northern and from the beginning of the Middle to the end of the central areas of Taimyr. The clastic material came Late Triassic. The obtained data indicate that terrige from the south and southeast. By the end of the Mid nous material carried from the Uralian fold belt dle Triassic, the Hercynian and Neoproterozoic prov reached the Franz Josef Land Archipelago no later enances remained the main sources of clastic material. than in the Middle Triassic and was transferred to Magmatic rocks presumably related to the Siberian Svalbard only in the Late Triassic (Riis et al., 2008; plume (250–220 Ma) and Paleo and Mesoprotero Bue et al., 2011; Bue and Andersen, 2013). Triassic zoic rocks of the East European Craton (Baltica) sediments of the Franz Josef Land Archipelago were began to erode. Transport of zircon from the typical deposited in a single North Barents Basin, and their Caledonian structures increased. Its possible sources formation was not related to the evolution of the Sve were late Timanides, Polar Urals, and Severnaya Zem drup Basin. lya. At the beginning of the Late Triassic, rocks related Paleogeographic reconstructions for the Barents to the Siberian plume, Hercynian and Caledonian Sea region were previously based mainly on the litho structures continued to supply clastic material, while logical, mineralogical, biostratigraphic, and seismic the transport from Paleo, Meso, and Neoprotero data (Ronkina and Vishnevskaya, 1981, 1982; Pche zoic structures virtually ceased. By the end of the Tri lina, 1985; Mørk, 1999; Kosteva, 2004; Petrov et al., assic, the erosion of Siberian traps and Hercynian 2008; Basov et al., 2009). It was proposed that the rocks decreased, giving way to the Caledonian com Franz Josef Land Basin in the Triassic was fed from the plexes, as well as Paleo, Meso, and Neoproterozoic northern MidArctic land (Lomonosov Ridge) structures. (Ronkina and Vishnevskaya, 1981, 1982; Kosteva, (3) The main sources of clastic material for the 2004). However, this conclusion is not confirmed by North Barents Sea sedimentary basin in the Middle– our data. Their comprehensive analysis showed that Late Triassic were structures of the Uralian fold belt. detrital material was transported to the Barents Sea Terrigenous material was presumably also supplied Basin by the Severnaya Zemlya mountain system, as from the East European Craton (Baltica), Timanides, well as Novaya Zemlya–Uralian, Baltic, and West Taimyr, and rocks of the Siberian plume. The material Svalbard paleolands (Basov et al., 2009). The obtained was mainly delivered from the south and southeast. U–Pb data on detrital zircon are wellconsistent with Influence of the Neoproterozoic sources systemati these paleogeographic reconstructions (Basov et al., cally decreased, while the role of the Caledonian 2009). In recent years, the paleogeographic recon sources increased from the beginning of the Middle to structions for Arctic regions were verified by the U/Pb the end of the Late Triassic. The U/Pb zircon dating age data on detrital zircon (Miller et al., 2006; Pease et shows that sediments derived from the Uralian fold al., 2007; Petrov, 2010; Bue et al., 2011; Omma et al., belt reached the Franz Josef Land Archipelago by the 2012; Miller et al., 2013; Bue and Andersen, 2013). Middle Triassic and accumulated in a single northern These data together with the results presented in this Barents Sea Basin.

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ACKNOWLEDGMENTS Gee, D.G., Beliakova, L., Pease, V., et al., New single zir con (Pbevaporation) ages from Vendian intrusions in the We are grateful to I.S. Ipat’eva (Geological Insti basement beneath the Pechora Basin, northeastern Baltica, tute, Moscow) for help in obtaining and processing Polarforschung, 2000, vol. 68, p. 161–170.11. data used in the paper. A.V. Maslov is thanked for Gehrels, G., Detrital zircon UPb geochronology: current comments, which greatly improved our manuscript. methods and new opportunities, Recent Advances in Tecton This work was financially supported by the Norwe ics of Sedimentary Basins, Busby, C. and Azor, A., Eds., gian Petroleum Directorate, the Earth Science Divi WileyBlackwell 2011, pp. 47–62. sion of the Russian Academy of Sciences (program Gehrels, G.E., Valencia, V., and Ruiz, J., Enhanced preci nos. 4 and 6), and the Russian Foundation for Basic sion, accuracy, efficiency, and spatial resolution of UPb Research (project no. 140593092 Norw_a). ages by laser ablationmulticollectorinductively coupled plasmamass spectrometry, Geochem., Geophys., Geosys tems, 2008, vol. 9, p. Q03017. doi:10.1029/2007GC001805. REFERENCES Gramberg, I.S., Shkola, I.V., Bro, E.G., et al., Parametric boreholes on islands in the Barents and Kara seas, Sov. 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