Geochemical Journal, Vol. 50, pp. 197 to 210, 2016 doi:10.2343/geochemj.2.0405

Geochemistry of Late Cambrian-Early Ordovician fluvial to shallow marine sandstones, western , : Implications for provenance, weathering, tectonic settings, and chemostratigraphy

S. A. MAHMUD,1* S. NASEEM,2 M. HALL1 and KHALID A. ALMALKI3

1School of Earth, Atmosphere and Environment, Monash University, Clayton, VIC 3800, Australia 2Department of Geology, University of Karachi, Pakistan 3King Abdulaziz City for Science and Technology, Saudi Arabia

(Received March 3, 2015; Accepted November 5, 2015)

A geochemical study of the Late Cambrian-Early Ordovician sandstones exposed in the , Tasmania, Australia, was carried out to develop an understanding of the provenance and tectonic settings. The average composition

of these sandstones displayed high SiO2 (92.72%), moderate Al2O3 (3.34%) and Fe2O3 (1.71%), low K2O (0.90%) and MgO (0.15%), and very low CaO and Na2O (<0.01%) concentrations. The sandstones were mainly classified as quartzarenite, and some samples were classified as sublitharenite. Tectonic discrimination diagrams based on major and trace elements

suggest passive margin settings. Provenance diagram (Al2O3 vs. TiO2) revealed that the Owen Group was derived from a silica-rich source. The average chemical index of alteration (CIA) was 78.45, indicating that the source area suffered severe weathering due to persistent warm and humid climate. High amounts of rare earth elements (REE) and strong negative anomalies on the chondrite-normalized REE pattern indicate an oxidizing deposition environment. The trace element chemostratigraphy reflects sharp contrasts in concentrations, distinguishing between the lower and upper sequences and also shows the effect of alteration assemblages.

Keywords: geochemistry, sandstones, provenance, weathering, Tasmania

between 494 Ma and 462 Ma. INTRODUCTION The Late Cambrian-Early Ordovician siliciclastics in The Late Cambrian-Early Ordovician syn-rift western Tasmania have a varied nomenclature history. siliciclastic depositional system (Owen Group) is mainly Initially described Owen Conglomerate by Officer and comprised of conglomerate, sandstone, and shale Hogg (1985), it was later referred West Coast Range Con- lithofacies. The Owen Group is widely distributed in glomerate by Conolly (1947). Subsequently it was ranked western and northern Tasmania (Fig. 1), where the main as a Group (Corbett, 1990), equivalent to the Denison exposures lie in an arcuate belt extending north-south Group, by Corbett et al. (1993) and Corbett and Turner along the West Coast Range before swinging to the north- (1989). The most widely accepted scheme for the inter- east, east-west, and eventually southeast at Mount Roland nal classification was proposed by Wade and Solomon and the Gog Range (Berry and Harley, 1983; Burns, 1964; (1958) and followed by Corbett (2001, 2004, 2014) and Corbett, 1975). The sequence overlies middle to Late Noll and Hall (2003, 2005, 2006) who classified the group Cambrian Volcanics (MRV), which also ac- into: (1) Lower Owen Conglomerate, (2) Middle Owen cumulated in a narrow arcuate zone around the present- Sandstone, (3) Middle Owen Conglomerate, and (4) Up- day western and northern margins of the Tyennan Block, per Owen Sandstone. This is generally regarded as the adjacent to the West Coast Range. Based on well-con- classic Owen Group stratigraphy and has been applied in strained dates from the underlying MRV (McNeill et al., the West Coast Range both north and south of the type 2012; McClenaghan et al., 2008; Perkins and Walshe, area at Mt. Owen, near Queenstown in western Tasma- 1993) and overlying Gordon Group (Berry, 1994; Ross nia. and Ross, 2007), the estimated age of the Owen Group is Recent studies by the authors (Driscoll et al., 2013; Mahmud et al., 2013) in the West Coast Range immedi- ately south of the have established stratigraphy markedly different from that in the type area (Mt. Owen) *Corresponding author (e-mail: [email protected]) and one that varies dramatically between different Copyright © 2016 by The Geochemical Society of Japan. depocenters controlled by syn-depositional faulting in

197 Fig. 1. Geological map of western Tasmania, showing the distribution of Late Cambrian-Early Ordovician sediments (after Brown et al., 2001).

198 S. A. Mahmud et al. ea.

Fig. 2. Geological map of the study ar

Geochemistry of Owen Group Siliciclastics, Tasmania, Australia 199 western Tasmania. The Owen Group exposed in the Mt. Jukes-Mt. Darwin area has been classified into two fin- ing up sequences, separated by a prominent unconformity (Fig. 2). However, in the Mt. Sorell-Mt. Strahan area, it is only comprised of a monotonous sandstone-conglom- erate sequence. Chemical composition (major and trace elements) of clastic sediments is widely used to evaluate provenance, tectonic settings, weathering, and climatic conditions (Banerjee and Banerjee, 2010; Caracciolo et al., 2011; Perri, 2014; Perri et al., 2012b, 2013, 2015a, 2015b, 2015c). Immobile trace elements such as Ti, Zr, Hf, Y, Sc, Th, Cr, and Co and rare earth elements (REE) are also good indicators of geological processes, provenance, and tectonic settings (Liu et al., 2007; Parisi et al., 2011; Perri et al., 2011a, 2011b, 2012a). Chemostratigraphy is a stratigraphic method based on variations in whole-rock geochemistry and is an effective tool for geochemical fin- gerprinting used for zonation and stratigraphic correla- tions (Weissert et al., 2008; Perri et al., 2015b). This study presents the chemical composition, includ- ing major, trace, and rare earth elements, of the Owen Group in the Mt. Jukes-Mt. Darwin and Mt. Sorell areas. The paper discusses various processes associated with the source rock, depositional settings, weathering, and diagenesis that might have affected Owen Group sediments. It also briefly presents trace element and REE chemostratigraphy of the Owen Group sediments for the Proprietary Peak section (Fig. 3).

REGIONAL GEOLOGY The Tyennan Orogeny in the Middle Cambrian was followed by the accumulation of MRV in much of west- ern Tasmania. Continuing extension and related uplift over a wider area lead to the formation of north-south trending troughs that were filled with debris and sediments de- rived from the adjacent Proterozoic basement (Berry and Bull, 2012; Seymour et al., 2007). The Owen Group in the West Coast Range is overlaid by Middle Ordovician Pioneer Sandstone and Gordon Limestone that were de- posited during a regional transgression that marked the onset of marine conditions following the end of rifting (Noll and Hall, 2003). The Owen Group sediments were deformed during the Middle to Late Devonian Tabberabberan Orogeny; D1 compressional deformation caused the formation of re- gional, upright, open north-south trending folds F1, mainly as inversion of structures associated with the re- versal of late Cambrian normal faults (Noll and Hall, 2005, 2006). In the East Jukes area, Noll and Hall (2005) describe a west-dipping reverse fault, along the western margin of , as a major basin boundary fault Fig. 3. Proprietary Peak stratigraphic section showing sam- that now juxtaposes an originally down thrown Owen ple locations.

200 S. A. Mahmud et al. Fig. 4. Plots of trace elements of sandstone samples on a ro- tated space diagram (Principle Component Analysis; PCA).

Group and MRV against Silurian and Devonian sediments. The younger D2 compressional deformation refolded and reoriented many D1 structures, forming north-north- west to northwest trending upright folds (F2). Major D2 folding is also widespread throughout western Tasmania and is accompanied by northwest striking reverse faults and thrusts (Cox, 1981; Noll and Hall, 2005). The over- printing of first-generation structures has resulted in a locally complex structural geometry in the West Coast Range, including dome and basin fold interference pat- terns (Noll and Hall, 2005, 2006).

MATERIALS AND METHOD

Sample selection Fig. 5. Classification of Owen Group sandstones: (a) log(Na O/ Twenty-four (24) representative samples from the 2 K2O) vs. log(SiO2/Al2O3) diagram (after Pettijohn et al., 1972), Owen Group were selected in and around the study area, and (b) log(Fe2O3/K2O) vs. log (SiO2/Al2O3) diagram (after with one complete succession of 13 samples selected from Herron, 1988). a measured section at Proprietary Peak, just north of Mt. Jukes, for chemostratigraphic evaluation.

Methodology 1996). Pure element oxide mixes in pure silica, along with Analysis of major elements was performed at the International and Tasmanian reference rocks, were used School of Earth Sciences - CODES, University of Tas- with numerous checks of reference rocks and pure silica mania. A half-gram (0.5 g) sample was mixed with 4.5 g blanks were run with each program. Corrections for mass flux (Lithium Tetraborate-Metaborate mix) for decompo- absorption were calculated using PANalytical Super-Q sition in a platinum crucible. Sulphide bearing samples software with its classic calibration model and alpha co- usually have a different mix with more LiNO3 as an oxi- efficients. dizing agent, the mix was pre-ignited at 700∞C for 10 min. Rare earth and selected trace element analysis was Iodine vapor was used as a releasing agent to remove discs performed at Monash University’s School of Earth, At- from the mold. Major elements were measured using mosphere and Environment, using a Thermo Finnigan X PANalytical Axios Advanced X-Ray Spectrometer series II, quadruple ICP-MS. Sample solutions were pro- (Robinson, 2003) 32 mm diameter pressed powder pills duced from approximately 50 mg of sample powder us- (10 g, 3.5 tons/cm–2) in a sample binder PVP-MC (Watson, ing high-pressure digestion methods. ICP-MS count rates

Geochemistry of Owen Group Siliciclastics, Tasmania, Australia 201 Fig. 6. Classification of Owen Group sandstones on K2O vs. Na2O plots (after Crook, 1974).

were externally standardized by calibration curves based on the in-house standard basalt BNB. Drift corrections were applied by the combined use of In and Bi as internal standards and the repeated analysis of dummy standards throughout the analytical session. Reproducibility of rep- licate analyses and accuracy was on the order of 5% for all elements.

RESULTS AND DISCUSSIONS Major elements Silica oxide (SiO2) was the most abundant oxide, rang- ing from 98.47 to 71.27%, with an average of 92.72%. Alumina (Al2O3) and iron (Fe2O3) oxides showed a simi- lar distribution pattern and ranged between 0.13–12.02%. Fig. 7. Plots of major element compositions of Owen Group The amount of potassium oxide (K2O) varied between 0.07–4.29%. Magnesium oxide (MgO) was low (0.15%). sandstones: (a) Fe2O3+MgO vs. TiO2, and (b): Fe2O3+MgO vs. Al2O3/SiO2 (after Bhatia, 1983). The amounts of CaO and Na2O were also very low, and their concentrations in most samples were less than 0.01%. Intense weathering in the study area probably resulted in their removal. The mean contents of TiO2, MnO, and P2O5 data of the present study revealed two major groups of were also very low at 0.21, 0.13, and 0.02% respectively. trace elements. Group I consisted of 21 elements that exhibited high positive loadings in the rotated space dia- Trace elements gram (Fig. 4). The strongest correlations of Zn (0.95), Sb Multivariate statistical approaches such as Principal (0.94), U (0.94), Sn (0.93), Pb (0.93), Y (0.93), As (0.93), Component Analysis (PCA) were used to reveal any pos- Cs (0.93), Th (0.93), Ta (0.92), Nb (0.92), Hf (0.91), Rb sible groupings of the samples based on their bulk com- (0.91), Tl (0.91), Be (0.91), Li (0.90), and Cd (0.90) indi- position. PCA facilitates the study of trace element data cate that the concentrations of all these elements supports by establishing groups and relationships among elemen- each other. They also reflect a strong affiliation with very tal compositions (Abdi and Williams, 2010; von Eynatten high silica concentrations, probably associated with the et al., 2003; Perri and Ohta, 2014). PCA of the elemental provenance. Strong loadings of Mo (0.89), Ga (0.87), and

202 S. A. Mahmud et al. Fig. 8. Ternary plot Th-Sc-Zr/10 of sandstone samples from the study area (after Bhatia and Crook, 1986).

Zr (0.84) are indicative of intense weathering, recycling, and redox conditions. Members of the second group showed an inverse nature compared to Group I: high nega- tive loading in the rotated space (Fig. 4). Nickel (–0.91), Co (–0.93), V (–0.92), Sr (–0.83), Ba (–0.74), Cu (–0.85), and Sc (–0.75) faced resistance from Group I in terms of concentration levels. The second group of elements was most likely associated with alteration assemblages, which are inferred to have caused late stage diagenesis in the study area.

Sandstone classification The relative concentrations of three major oxide groups (silica and alumina oxides, alkali oxides, and iron oxide plus magnesia) can be utilized to classify sandstones (Herron, 1988). The Al2O3/SiO2 ratio indicates the ex- tent of feldspar leaching and subsequent enrichment of silica, while the K2O/Na2O ratio is attributed to the preva- lence common presence of K-bearing minerals such as K-feldspar, mica, illite, muscovite, and biotite (Sahraeyan and Bahrami, 2012). The diagram of log(Na2O/K2O) vs. log(SiO2/Al2O3) exhibits a linear trend, representing quartzarenite, sublitharenite, and subarkosic compositions of Owen Group sandstones (Fig. 5a). The diagram of log(Fe2O3/K2O) vs. log(SiO2/Al2O3) shows that the ma- jority of the samples are quartzarenites, while some are sublitharenite, subarkose, and Fe-sand (Fig. 5b). The K2O/ Na2O ratio, described by Crook (1974) as a useful tool to classify the nature of sandstones, plots the Owen Group samples in the quartz-rich field (Fig. 6). Fig. 9. (a) SiO2 vs. Al2O3 + K2O + Na2O, showing chemical maturity (after Suttner and Dutta, 1986); (b) ternary 15Al-300Ti- Tectonic setting Zr plots of sandstone in the study area (after Garcia et al., Stable and immobile element groups in clastic sedi- 1991); (c) Th/Sc vs. Zr/Sc plots (after McLennan et al., 1993).

Geochemistry of Owen Group Siliciclastics, Tasmania, Australia 203 Table 1. Major oxide composition of Owen Group (% wt)

Sample SiO2 TiO2 Al2O3 Fe2O3 MnO MgO CaO Na2OK2OP2O5 LOI B19 Purplish/Pinkish Sandstone (L8) 71.27 0.27 12.02 8.76 0.01 0.70 0.01 0.01 4.29 0.04 2.37 B20 White/Grey Sandstone-Cong. (L9) 92.51 0.25 3.25 1.76 0.01 0.17 0.01 0.01 1.09 0.01 0.63 B21 Lower Pink Sandstone (L10) 89.08 0.37 5.63 1.91 0.01 0.16 0.01 0.01 1.65 0.02 0.90 B11 Upper (L) Pink Sandstone (L12) 88.58 0.19 7.16 1.90 0.01 0.03 0.01 0.01 0.26 0.02 1.44 B15 Upper (L) Pink Sandstone (L12) 91.66 0.48 3.70 1.92 0.01 0.12 0.01 0.02 1.01 0.04 0.65 B18 Interbedded Sandstone Shale (L13) 91.89 0.29 3.91 1.66 0.01 0.13 0.01 0.02 1.12 0.02 0.68 A01 Purple Conglomerate (U1) 90.48 0.13 2.45 5.39 0.01 0.05 0.01 0.01 0.63 0.04 0.46 A04 Upper Pink Sandstone (U2) 98.13 0.04 0.44 0.77 0.01 0.01 0.01 0.01 0.11 0.01 0.20 A05 Upper Pink Sandstone (U2) 97.82 0.07 0.78 0.91 0.01 0.02 0.01 0.01 0.22 0.01 0.21 A14 Upper White Conglomerate (U3) 91.73 0.36 4.40 0.95 0.01 0.28 0.01 0.01 1.42 0.04 1.05 A19 Interbedded Unit (U4) 93.31 0.14 1.99 3.25 0.01 0.16 0.01 0.01 0.66 0.01 0.55 C13 Interbedded Unit (U4) 93.91 0.08 1.25 3.26 0.01 0.09 0.01 0.01 0.45 0.01 0.50 A09 Lower White Cong/Grey SSt (L1) 92.85 0.30 3.56 1.50 0.01 0.15 0.01 0.01 1.10 0.01 0.69 A11 Lower Pink Sandstone (L3) 98.32 0.11 0.22 0.15 0.01 0.01 0.01 0.01 0.07 0.01 0.13 C17 Lower Pink Sandstone (L7) 92.48 0.38 4.23 1.82 0.01 0.03 0.01 0.01 0.10 0.01 0.78 C21 White Conglomerate (L6) 91.96 0.36 3.95 0.68 0.01 0.36 0.01 0.01 1.29 0.01 0.96 B25 Sorell Sandstone 96.45 0.12 1.73 0.34 0.01 0.13 0.01 0.01 0.53 0.01 0.45 B01 Sorell Sandstone 93.53 0.17 3.68 0.39 0.01 0.20 0.01 0.01 1.11 0.01 0.81 B03 Sorell Sandstone 93.77 0.19 3.40 0.35 0.01 0.20 0.01 0.01 0.98 0.01 0.76 B36 Strahan Sandstone 98.14 0.08 0.74 0.13 0.01 0.05 0.01 0.01 0.22 0.01 0.22 B38 King River/Strahan Sandstone 89.51 0.30 6.19 0.58 0.01 0.28 0.01 0.03 1.81 0.01 1.04 B05 Basal Darwin Haematitic Sandstone 93.77 0.19 3.40 0.35 0.01 0.20 0.01 0.01 0.98 0.01 0.76 B06 Purple Conglomerate (South Darwin Peak) (U1) 95.86 0.12 1.58 2.01 0.01 0.03 0.01 0.01 0.47 0.03 0.31 B08 Upper Pink Sandstone (South Darwin Peak) (U2) 98.47 0.05 0.58 0.30 0.01 0.02 0.01 0.01 0.19 0.01 0.15

Fig. 10. Chondrite-normalized REE patterns of Owen Group sandstones.

204 S. A. Mahmud et al. Table 2. Trace element composition of the Owen Group, Tasmania, Australia (mg/kg)

Sample Li Be Sc V Cr Co Ni Cu Zn Ga As Rb Sr Y B19 Purplish/Pinkish Sandstone (L8) 12.4 3.7 3.1 30.9 29.7 3.7 3.3 4.4 89.7 25.2 2.6 144 232 38.0 B20 White/Grey Sandstone-Cong. (L9) 15.4 4.5 2.4 16.7 22.6 1.9 0.9 2.2 99.3 29.5 3.0 179 181 43.9 B21 Lower Pink Sandstone (L10) 16.5 4.9 2.4 11.1 47.3 1.5 0.9 1.9 93.1 26.0 3.3 179 83.4 44.5 B11 Upper (L) Pink Sandstone (L12) 16.2 4.9 1.9 7.4 26.8 1.1 0.6 0.2 89.0 26.7 3.2 176 57.1 42.4 B15 Upper (L) Pink Sandstone (L12) 16.2 4.9 1.9 7.4 26.8 1.1 0.6 0.2 89.0 26.7 3.2 176 57.1 42.4 B18 Interbedded Sandstone Shale (L13) 26.7 8.5 1.5 1.9 37.0 0.6 0.9 1.0 106 29.8 5.3 234 4.7 60.3 A01 Purple Conglomerate (U1) 28.6 9.8 2.1 5.1 12.6 1.0 0.5 0.9 130 35.2 6.1 284 22.9 77.3 A04 Upper Pink Sandstone (U2) 27.0 8.2 1.7 1.8 32.4 0.6 0.6 0.6 110 31.2 5.1 232 10.0 61.1 A05 Upper Pink Sandstone (U2) 11.7 3.6 3.1 33.3 30.8 3.9 3.2 4.8 85.5 25.0 2.7 141 257 37.4 A14 Upper White Conglomerate (U3) 28.2 8.6 1.7 1.6 32.6 0.6 0.5 1.0 108 30.6 5.4 237 7.2 61.9 A19 Interbedded Unit (U4) 12.8 3.8 2.0 11.3 35.5 1.5 0.9 1.0 80.4 25.3 2.8 152 105 37.3 C13 Interbedded Unit (U4) 41.1 12.4 1.1 0.6 49.5 0.4 0.8 0.4 139 36.2 9.0 343 3.6 88.7 A09 Lower White Cong/Grey SSt (L1) 15.3 4.2 2.2 11.8 26.5 1.5 0.8 2.0 87.3 26.2 2.9 163 102 41.8 A11 Lower Pink Sandstone (L3) 27.5 8.2 1.7 3.3 30.0 0.8 0.5 1.5 107 30.9 5.3 238 26.6 59.7 C17 Lower Pink Sandstone (L7) 8.5 2.3 3.4 26.3 11.6 2.7 0.7 4.0 79.5 22.3 1.4 106 366 32.0 C21 White Conglomerate (L6) 48.1 15.1 0.9 0.5 59.5 0.4 0.8 0.6 158 37.8 11.0 394 1.3 103 B25 Sorell Sandstone 14.2 4.1 2.2 15.1 14.1 1.8 0.9 1.4 85.6 26.2 2.9 159 128 40.7 B01 Sorell Sandstone 13.7 4.1 2.3 12.8 6.6 1.7 0.9 2.0 84.0 26.5 2.8 160 111 41.0 B03 Sorell Sandstone 17.1 4.9 2.1 11.4 20.9 1.4 0.7 2.1 88.0 26.9 3.7 176 123 41.7 B36 Strahan Sandstone 51.1 15.9 0.9 0.5 72.8 0.4 0.9 0.5 161 37.7 11.6 408 0.9 107 B38 King River/Strahan Sandstone 30.6 9.2 1.5 1.2 20.2 0.5 0.4 0.3 112 31.6 5.5 244 4.9 64.5 B05 Basal Darwin Haematitic Sandstone 40.5 12.5 1.0 0.6 48.0 0.4 0.7 0.4 139 35.2 8.9 343 5.6 88.5 B06 Purple Conglomerate (South Darwin Peak) (U1) 18.1 5.4 2.1 7.2 42.2 1.1 0.9 1.9 94.5 28.0 3.5 190 50.8 46.6 B08 Upper Pink Sandstone (South Darwin Peak) (U2) 11.4 3.5 3.5 38.0 27.0 4.6 4.0 5.4 86.2 24.7 2.4 138 256 37.5

Sample Zr Nb Mo Cd Sn Sb Cs Ba Hf Ta Tl Pb Th U B19 Purplish/Pinkish Sandstone (L8) 124 5.9 0.2 4.4 0.3 1.2 491 15.8 7.2 0.2 9.1 17.0 4.4 770 B20 White/Grey Sandstone-Cong. (L9) 149 7.4 0.3 5.9 0.4 1.5 482 19.5 7.8 0.2 11.2 20.0 5.4 975 B21 Lower Pink Sandstone (L10) 151 7.9 0.3 4.9 0.3 1.5 211 19 8.1 0.2 10.3 20.0 5.3 1003 B11 Upper (L) Pink Sandstone (L12) 147 7.8 0.3 5.0 0.3 1.5 148 18.3 7.9 0.2 9.8 20.0 5.3 924 B15 Upper (L) Pink Sandstone (L12) 147 7.8 0.3 5.0 0.3 1.5 148 18.3 7.9 0.2 9.8 20.0 5.3 924 B18 Interbedded Sandstone Shale (L13) 230 13.0 0.3 7.9 0.5 2.5 7.5 24.5 12.4 0.2 13.2 35.0 9.0 1138 A01 Purple Conglomerate (U1) 293 10.8 0.3 10.2 0.7 2.9 52.0 28.2 15.9 0.2 14.6 44.0 11.2 1228 A04 Upper Pink Sandstone (U2) 239 12.3 0.3 8.0 0.5 2.5 7.9 24.7 12.7 0.2 13.3 35.0 8.6 1147 A05 Upper Pink Sandstone (U2) 121 5.8 0.2 4.1 0.3 1.1 530 15.7 7.0 0.2 8.8 17.0 4.3 764 A14 Upper White Conglomerate (U3) 242 12.9 0.3 8.0 0.6 2.6 6.7 25.0 13.0 0.2 13.4 36.0 8.9 1168 A19 Interbedded Unit (U4) 124 6.2 0.2 4.2 0.3 1.2 291 16.8 7.2 0.2 9.2 18.0 4.5 841 C13 Interbedded Unit (U4) 356 20.4 0.5 12.7 0.9 4.1 0.8 35.8 20.0 0.4 19.9 61.0 15.0 1433 A09 Lower White Cong/Grey SSt (L1) 138 7.2 0.3 4.7 0.3 1.4 268 18.0 7.9 0.2 10.3 19.0 5.0 935 A11 Lower Pink Sandstone (L3) 233 12.7 0.3 7.6 0.5 2.4 70 24.7 13.0 0.2 13.3 34.0 8.9 1182 C17 Lower Pink Sandstone (L7) 88.5 3.9 0.2 2.6 0.2 0.7 927 10.2 5.0 0.1 6.9 9.9 2.6 524 C21 White Conglomerate (L6) 409 23.0 0.5 15.2 1.1 5.1 1.4 41.2 21.4 0.4 23.3 70.0 18.2 1608 B25 Sorell Sandstone 134 6.9 0.2 4.5 0.3 1.3 328 17.5 7.5 0.2 9.8 19.0 4.9 890 B01 Sorell Sandstone 136 6.8 0.2 4.4 0.3 1.3 282 17.7 7.7 0.1 9.4 18.0 4.9 918 B03 Sorell Sandstone 153 8.0 0.3 4.8 0.3 1.5 336 18.0 8.6 0.2 10.8 20.0 5.3 925 B36 Strahan Sandstone 441 23.4 0.5 16.2 1.2 5.4 1.3 43.5 24.3 0.5 24.4 72.0 19.3 1674 B38 King River/Strahan Sandstone 254 13.8 0.3 8.5 0.6 2.7 3.2 25.2 13.5 0.2 13.7 39.0 9.6 1134 B05 Basal Darwin Haematitic Sandstone 355 20.2 0.4 12.7 0.9 4.1 1.6 35.7 19.3 0.4 19.8 61.0 15.1 1425 B06 Purple Conglomerate (South Darwin Peak) (U1) 168 9.0 0.3 5.6 0.4 1.7 132 19.6 9.2 0.1 10.6 23.0 5.9 1003 B08 Upper Pink Sandstone (South Darwin Peak) (U2) 117 5.6 0.2 4.0 0.3 1.1 495 14.6 6.7 0.1 8.5 16.0 4.1 729

mentary rocks are significant for appraising tectonic en- sediments have low Ti and high Zr concentrations (Ti/Zr vironments because these elements are least affected by ratio < 10). The average Ti/Zr ratio of the Owen Group weathering and alteration processes (McLennan et al., samples was 1.31, categorizing them as passive margin 1993; Roser and Korsch, 1986). Bhatia (1983) uses Fe2O3 deposits. These tectonic discrimination diagrams are + MgO vs. TiO2 and Al2O3/SiO2 diagrams to discrimi- widely used and are reliable indicators of tectonic set- nate among various tectonic settings. The Owen Group tings in most cases. The tectonic setting of clastic rocks sandstone samples mainly plot in the passive continental can also be evaluated using the Th-Sc-Zr/10 ratio (Perri margin field, with a few exceptions (Figs. 7a and b). et al., 2011a). The Th-Sc-Zr/10 diagram plots the Owen Sediments related to passive continental margins are ma- Group sandstone samples close to the passive margin set- ture and are usually deposited in intracratonic basins ting (Fig. 8). For Owen Group sediments, an exception- (Sahraeyan and Bahrami, 2012). In general, such ally quartz-rich provenance and warm/humid depositional

Geochemistry of Owen Group Siliciclastics, Tasmania, Australia 205 Table 3. Rare Earth Elements (REE) of the Owen Group, Tasmania, Australia (mg/kg)

Sample La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu B19 Purplish/Pinkish Sandstone (L8) 103 185 19.0 65.0 11.0 2.3 9.2 1.4 7.4 1.5 3.7 0.5 3.2 0.5 B20 White/Grey Sandstone-Cong. (L9) 118 214 22.0 73.0 12.0 2.5 10.0 1.5 8.3 1.6 4.3 0.6 3.8 0.6 B21 Lower Pink Sandstone (L10) 116 207 21.0 70.0 12.0 1.6 9.8 1.5 8.0 1.6 4.2 0.6 3.7 0.5 B11 Upper (L) Pink Sandstone (L12) 112 201 20.0 67.0 12.0 1.4 9.3 1.4 7.7 1.5 4.1 0.6 3.6 0.5 B15 Upper (L) Pink Sandstone (L12) 112 201 20.0 67.0 12.0 1.4 9.3 1.4 7.7 1.5 4.1 0.6 3.6 0.5 B18 Interbedded Sandstone Shale (L13) 165 289 29.0 92.0 15.0 0.8 13.0 1.9 11.0 2.2 5.8 0.8 5.2 0.8 A01 Purple Conglomerate (U1) 216 362 37.0 118 20.0 1.0 16.0 2.5 14.0 2.8 7.3 1.0 6.6 0.9 A04 Upper Pink Sandstone (U2) 172 300 30.0 94.0 16.0 0.7 13.0 1.9 11.0 2.2 5.7 0.8 5.2 0.7 A05 Upper Pink Sandstone (U2) 98.9 179 19.0 62.0 11.0 2.4 8.9 1.3 7.3 1.4 3.7 0.5 3.2 0.5 A14 Upper White Conglomerate (U3) 172 300 30.0 94.0 16.0 0.7 13.0 1.9 11.0 2.2 5.8 0.8 5.3 0.8 A19 Interbedded Unit (U4) 104 193 19.0 64.0 11.0 2.0 8.8 1.3 7.1 1.4 3.7 0.5 3.3 0.5 C13 Interbedded Unit (U4) 275 471 46.0 141 23.0 0.7 19.0 2.9 16.0 3.2 8.7 1.2 8.0 1.2 A09 Lower White Cong/Grey SSt (L1) 113 192 21.0 70.0 12.0 2.0 9.4 1.4 7.9 1.5 4.0 0.6 3.5 0.5 A11 Lower Pink Sandstone (L3) 164 288 29.0 92.0 15.0 1.0 13.0 1.9 11.0 2.2 5.7 0.8 5.2 0.8 C17 Lower Pink Sandstone (L7) 91.5 159 17.0 63.0 11.0 2.9 8.6 1.2 6.5 1.2 3.0 0.4 2.4 0.4 C21 White Conglomerate (L6) 265 463 45.0 139 24.0 0.6 20.0 3.1 18.0 3.7 10.0 1.4 9.2 1.3 B25 Sorell Sandstone 109 193 20.0 67.0 12.0 2.0 9.3 1.4 7.6 1.5 3.9 0.5 3.4 0.5 B01 Sorell Sandstone 106 189 20.0 65.0 11.0 1.9 9.2 1.4 7.4 1.5 3.8 0.5 3.4 0.5 B03 Sorell Sandstone 116 201 20.0 68.0 11.0 1.9 9.3 1.4 7.6 1.5 4.0 0.5 3.5 0.5 B36 Strahan Sandstone 254 443 44.0 136 24.0 0.6 20.0 3.2 19.0 3.8 10.0 1.5 9.6 1.4 B38 King River/Strahan Sandstone 182 322 32.0 99.0 16.0 0.7 13.0 2.0 11.0 2.3 6.1 0.8 5.5 0.8 B05 Basal Darwin Haematitic Sandstone 261 455 44.0 135 22.0 0.7 18.0 2.8 16.0 3.2 8.7 1.2 7.9 1.1 B06 Purple Conglomerate (South Darwin Peak) (U1) 126 220 23.0 75.0 13.0 1.4 10.0 1.5 8.5 1.7 4.5 0.6 4.0 0.6 B08 Upper Pink Sandstone (South Darwin Peak) (U2) 100 174 19.0 64.0 11.0 2.3 8.9 1.3 7.2 1.4 3.6 0.5 3.1 0.4

environment might have led to a compositionally unu- sediments were subjected to a high degree of weathering, sual example of a syntectonic (or active margin) deposit, resulting in removal of Ca, Na, and K-bearing minerals. rather than a typical passive margin quartzarenite. At this High CIA also reflects persistent warm and humid cli- stage we do not have firm evidence regarding the orien- matic conditions (Rahman and Suzuki, 2007). tation of the massive transgression associated with the The SiO2/Al2O3 ratio is sensitive to sediment recy- final stages of Owen Group deposition. It could have been cling and weathering processes and can be used as an in- a regular massive transgression affected by dicator of sediment maturity (Liu et al., 2007). These paleotopography in the region. values in unaltered igneous rocks range from ~3.0 (ba- sic) to ~5.0 (acidic), while values >5.0–6.0 in sediments Weathering are indicative of progressive maturity (Roser et al., 1996). The intensity of weathering is primarily a function of SiO2/Al2O3 ratios of the Owen Group ranged from 5.92 the rate of tectonic uplift and climatic conditions. During to 440.8, with an average of 69.4, indicating strong sedi- weathering, feldspars are easily chemically altered, re- ment maturity. sulting in the depletion of alkalis (Na and K) and alka- Suttner and Dutta (1986) proposed a bivariate plot line earth elements (Ca), with preferential enrichment of (SiO2 vs. Al2O3 + K2O + Na2O) to identify the level of Al2O3 (Nesbitt and Young, 1982; Cingolani et al., 2003). maturity and climatic conditions. Results of this plot (Fig. Weathering effects can be evaluated in terms of molecu- 9a) suggest a humid to semi-humid climate. The Owen lar percentages of oxides (Jafarzadeh and Hosseini-Barzi, Group had an average 92.72% SiO2 concentration, which 2008). Nesbitt and Young (1982) introduced an effective also suggests very high compositional maturity (Pettijohn, tool to quantify the degree of weathering, known as 1987). Initial composition of parent rock may be affected Chemical Index of Alteration (CIA), as defined by the during intense alteration, but the concentration of weath- molecular proportions: ering resistance elements remains constant. The ternary plot of Al-Ti-Zr is valuable for inferring the type of clas- CIA = Al2O3/(Al2O3 + CaO* + Na2O + K2O) ¥ 100 tic rock and may illustrate the presence of sorting-related fractionations (Garcia et al., 1991; Perri et al., 2011b, * represents the amount of CaO incorporated only in the 2013). Furthermore, the Zr/Sc vs. Th/Sc plot is used to silicate phases. evaluate sediment recycling and chemical differentiation This index provides a practical approach to measur- for clastic rocks (McLennan et al., 1993). Both Al-Ti-Zr ing the degree of alteration; higher CIA values represent (Fig. 9b) and Zr/Sc vs. Th/Sc (Fig. 9c) plots suggest re- greater weathering. The calculated CIA indices of the cycling effects for the studied rocks and show that these Owen Group sandstone samples ranged from 73.69 to are compositionally mature sediments. 97.66, with an average of 78.45. This suggests that the

206 S. A. Mahmud et al. The chondrite-normalized REE distribution pattern of the Owen Group samples illustrated a very strong nega- tive Eu anomaly (Fig. 10), which is attributable to the presence of Eu-depleted, silica-rich sediments (Banerjee and Banerjee, 2010; Gao and Wedepohl, 1995). Sediments deposited in reducing environments are characterized by low REE concentrations and a positive Eu anomaly, while sediments deposited in oxidizing conditions have a high total REE concentration and Eu depletion (Yanjing and Yongchao, 1997). The chondrite-normalized REE distri- bution suggests that the sediments might have been de- posited in a high oxidizing environment. Taylor and McLennan (1995) and Slack and Stevens (1994) have used REE data to appraise the age of source rocks. Sediments with negative Eu anomalies and Gd/Yb ratios <2.0 are characteristic of rocks from the post- Archean period (Mishra and Sen, 2012). The ratio Gd/Yb in the Owen Group varied between 2.04 and 3.54, indi- cating that the age of the major parent rocks is close to Proterozoic.

Chemostratigraphy Chemostratigraphy is a stratigraphic tool based on variations of whole-rock geochemistry; it uses chemical fingerprints stored in the sediments to evaluate variations in chemical compositions that signify changes associated with source rock characteristics and diagenetic processes (Weissert et al., 2008). In this study, selected trace ele- ment and REE concentrations and their ratios were used to visualize chemostratigraphic characteristics of the Owen Group sandstones in the Proprietary Peak section. Variation curves of selected elements were arranged from older to younger sequences (Figs. 11a and b). Almost all the elements showed a similar low distri- bution pattern, indicating the contribution of a massive silica-rich source. The younger samples displayed high variation in the concentration of elements, with Ba, Sr, and V showing opposite trends compared to other ele- ments. A strong negative correlation between Ba and Sr in the sandstones might reflect the alteration assemblages. Vanadium is sensitive to oxidation state of the depositional 2– basin and exists as vanadium oxyanions (HVO4 and – Fig. 11. Composite chemostratigraphy with (a) selected ele- H2VO4 ) in the oxic environment (Tribovillard et al., ments of the Owen Group and (b) selected elemental ratios of 2006). In reducing conditions, it may change to V (IV), the Owen Group. forming vanadyl ions (VO2–), and under strong reducing conditions it may change to V (III), forming vanadium hydroxide V(OH)3. The concentration curve of V displays low uniform abundance, again indicating a dominant oxi- Rare earth elements dizing environment, except for one sample of Upper Pink The REE concentrations in clastic rocks and Eu Sandstone (U2-A05). anomalies contribute information related to source rock Element group (Rb, Ga, Nb, La, and Ce) demonstrated characteristics (Cullers, 1994; Taylor and McLennan, two episodes of high enrichment. Since these elements 1995). REE data of the Owen Group sediments are re- are commonly found as trace elements in volcanic/felsic ported in Table 3. rocks, the abundances of these elements are probably due

Geochemistry of Owen Group Siliciclastics, Tasmania, Australia 207 to the existence of an MRV source and later diagenetic malized REE distribution patterns show a strong nega- alteration assemblages. tive Eu anomaly, suggesting that the sediments were de- The Th/Sc ratio is a good overall indicator of chemi- posited in a highly oxidizing environment. cal differentiation processes because Th is typically an The chemostratigraphy based on chemical variations incompatible element, whereas Sc is typically a compat- of trace and rare earth elements suggests obvious anoma- ible element (McLennan et al., 1993; Mongelli et al., lies and also marks the unconformity between the upper 2006). The Th/Sc ratios were consistent in the Owen and lower Owen Group sequences. Group sandstones. The Cr/Zr and Cr/Nb ratios had fluc- tuating trends, representing differential intensities of al- Acknowledgments—The authors would like to thank Dr. H. terations. Large ion lithophile elements (Sr and Rb) are Narita (Associate Editor, GJ) for editing and providing guid- associated with silica-rich rocks. The Rb/Sr ratio exhib- ance. Many thanks to Francesco Perri for reviewing the manu- ited a rapid decrease close to the Purple Conglomerate script and providing constructive feedback that improved the (U1) at the base of the upper sequence, probably due to article. Also, thanks are due to an anonymous reviewer. Dr. Mahmud is thankful to the School of Earth, Atmosphere and the influx of volcanic source grains. The ratio also re- Environment and to Monash University for providing the Post flects the unconformity between the lower and upper Publication Award. Khalid Almalki was supported by King Owen Group sequences. Abdulaziz City for Science and Technology. Gu et al. (2002) describes the La/Sc and Th/Sc ratios as effective tools to identify characteristics of source rocks. These ratios within the Owen Group demonstrated REFERENCES variability, indicating the influence of a secondary source, Abdi, H. and Williams, L. J. (2010) Principal component analy- in this case MRV. Liu et al. (2007) used the Ce/La and sis. Wiley Interdisciplinary Reviews: Comp. Stats. 2, 433– La/Yb ratios to assess homogenization and recycling of 459. sediments. The narrow ranges in the Ce/La and La/Yb Banerjee, A. and Banerjee, D. (2010) Modal analysis and ratios of the Owen Group indicate the effect of sedimen- geochemistry of two sandstones of the Bhander Group (Late tary recycling. Neoproterozoic) in parts of the central Indian vindhyan ba- sin and their bearing on the provenance and tectonics. J. Earth Sys. Sci. 119, 825–839. CONCLUSION Berry, R. F. (1994) Tectonics of western Tasmania; late Precambrian-Devonian. Contentious issues in Tasmanian This study documented, for the first time, the major, geology. G. Soc. Aust. 5–8. trace, and rare earth elemental data of sandstones of the Berry, R. F. and Bull, S. W. (2012) The pre-Carboniferous ge- Owen Group in the southern West Coast Range, Tasma- ology of Tasmania. Episodes: Int. G. Newsmagazine 35, nia. It presented a statistical approach that showed two 195–204. obvious element groups on a PCA diagram. This effec- Berry, R. F. and Harley, S. (1983) Pre-Devonian stratigraphy tively classified the elements associated with primary and structure of the Prion Beach-Rocky Boat Inlet- composition and those associated with alteration assem- Osmiridium Beach coastal section, southern Tasmania. Proc. blages. Royal Soc. Tas. 117, 59–75. Bhatia, M. R. (1983) Plate tectonics and geochemical compo- Several log plots, including log(Al2O3/SiO2) vs. log(K O/Na O), log(Fe O /K O) vs. log (SiO /Al O ), sition of sandstones. J. Geol., 611–627. 2 2 2 3 2 2 2 3 Bhatia, M. R. and Crook, K. A. (1986) Trace element charac- and K O vs. Na O, classified these sandstones primarily 2 2 teristics of graywackes and tectonic setting discrimination as quartzarenites with some sublitharenite, subarkosic, of sedimentary basins. Cont. Min. Petro. 92, 181–193. and Fe-sands. The SiO2 vs. Al2O3 + K2O + Na2O plot Brown, A. V., Calver, C. R., Clarke, M. J., Corbettt, K. D., reflects deposition in humid to semi-humid climatic con- Everard, J. L., Forsyth, S. M., Goscombe, B. A., Green, G. ditions and suggests that the sediments are R., McClenaghan, M. P., Pemberton, J. and Seymour, D. B. compositionally mature. (2001) 1:500,000 Digital Series The Fe2O3 + MgO vs. TiO2 plots and Al2O3/SiO2 ra- Mapsheet Tas. Geol. Survey. tios and the Sc/Cr vs. La/Y plots and Ti/Zr ratios show Burns, K. L. (1964) Devonport, Tasmania. Tasmania Depart- that the Owen Group was deposited in a passive margin ment of Mines Geological Atlas 1:63,360 Series Explana- setting. An exceptionally quartz-rich provenance and tory Report, 266. warm/humid depositional environment might have given Caracciolo, L., Le Pera, E., Muto, F. and Perri, F. (2011) Sand- stone petrology and mudstone geochemistry of the Peruc- rise to a compositionally unusual example of a syntectonic Korycany Formation (Bohemian Cretaceous Basin, Czech (or active margin) deposit, rather than a typical passive Republic). Int. Geol. Rev. 53, 1003–1031. margin quartzarenite. Cingolani, C. A., Manassero, M. and Abre, P. (2003) Composi- The CIA shows that the Owen Group sandstones ex- tion, provenance, and tectonic setting of Ordovician perienced severe weathering conditions. Chondrite-nor- siliciclastic rocks in the San Rafael block: Southern exten-

208 S. A. Mahmud et al. sion of the Precordillera crustal fragment, Argentina. J. S. sands and shales from core or log data. J. Sed. Res. 58. Am. Earth Sci. 16, 91–106. Jafarzadeh, M. and Hosseini-Barzi, M. (2008) Petrography and Conolly, H. J. C. (1947) Geology in exploration; geochemistry of Ahwaz Sandstone Member of Asmari For- example. Proc. Aust. Inst. Min. Metal. 146–147, 1–22. mation, Zagros, Iran: implications on provenance and tec- Corbett, K. D. (1975) The late Cambrian to early Ordovician tonic setting. Rev. Mex. de Ciencias Geol. 25, 247–260. sequence on the Denison Range, Southwest Tasmania. Proc. Liu, S., Lin, G., Liu, Y., Zhou, Y., Gong, F. and Yan, Y. (2007) Royal Soc. Tas. 109, 111–120. Geochemistry of Middle Oligocene-Pliocene sandstones Corbett, K. D. (1990) Cambro-Ordovician stratigraphy, West from the Nanpu Sag, Bohai Bay Basin (Eastern China): Coast Range to Black Bluff. Geology in Tasmania—A Implications for provenance, weathering, and tectonic set- Generalist’s Influence, Geol. Soc. Aust. Tas. Div., 8–13. ting. Geochem. J. 41, 359–378. Corbett, K. D. (2001) New mapping and interpretations of the Mahmud, S. A., Hall, M. and Driscoll, J. P. (2013) Correlating Mount Lyell mining district, Tasmania: a large hybrid Cu- fluvial sediments in rift systems: A case study of the late Au system with an exhalative Pb-Zn top. Econ. Geol. 96, Cambrian in Western Tasmania, Australia. Abstract: 10th 1089–1122. International Conference on Fluvial Sedimentology, Leeds, Corbett, K. D. (2004) Updating and revision of the 1:25000 U.K. (unpubl.). scale series geological maps covering the Mt Read Volcanics McClenaghan, M. P., Green, D., Seymour, D. B., Brown, A. V. belt in western and northwestern Tasmania. Tas. Geol. Surv. and Vicary, M. J. (2008) Digital Geological Atlas 1:25000 Rec. 3. Series, Sheet 4440 Gog, Min. Res. Tas. Corbett, K. D. (2014) A summary of Tasmania’s geology and McLennan, S., Hemming, S., McDaniel, D. and Hanson, G. geological history. Geological Evolution of Tasmania (1993) Geochemical approaches to sedimentation, prov- (Corbett, K. D., Quilty, P. G. and Calver, C. R., eds.), enance, and tectonics. Geol. Soc. Am. Spec. Pap. 284, 21– Geolgoical Society of Australia (Tasmania Devision), Spe- 40. cial Publication 24, 1–12. McNeill, A. W., Mortensen, J. K. and Gemmell, J. B. (2012) Corbett, K. D. and Turner, N. J. (1989) Early Paleozoic defor- High precison U-Pb chronostratigraphy of the Mount Read mation and tectonics. Sp. Pub. - Geol. Soc. Aust. 15, 154– Volcanics, Tasmania: Implications for mineral exploration 181. and tectonic reconstructions. Proc. Selwyn Symp. Geol. Soc. Corbett, K. D., Pemberton, J. and Vicary, M. J. (1993) Geology Aust. (unpubl.). of the Mt Jukes-Mt Darwin area. . Mishra, M. and Sen, S. (2012) Provenance, tectonic setting and Min. Res. Tas. Project Map 13. source-area weathering of Mesoproterozoic Kaimur Group, Cox, S. F. (1981) The stratigraphic and structural setting of the Vindhyan Supergroup, Central India. Geol. Acta 10, 283– Mt Lyell volcanic-hosted sulphide deposits. Econ. Geol. 76, 293. 231–245. Mongelli, G., Critelli, S., Perri, F., Sonnino, M. and Perrone, Crook, K. A. W. (1974) Lithogenesis and geotectonics: the sig- V. (2006) Sedimentary recycling, provenance and nificance of compositional varioations in flysh arenites paleoweathering from chemistry and mineralogy of (graywackes). Modern and Ancient Geosynclinal Sedimen- Mesozoic continental redbed mudrocks, Peloritani Moun- tation. Soc. Econ. Paleontol., Mineral. Special Publication tains, Southern Italy. Geochem. J. 40, 197. 19 (Dott, R. H. and Shaver, R. H., eds.), 304–310, SEPM. Nesbitt, H. and Young, G. (1982) Early Proterozoic climates Cullers, R. L. (1994) The chemical signature of source rocks in and plate motions inferred from major element chemistry size fractions of Holocene stream sediment derived from of lutites. Nature 299, 715–717. metamorphic rocks in the Wet Mountains region, Colorado, Noll, C. A. and Hall, M. (2003) Stratigraphic architecture and U.S.A. Chem. Geol. 113, 327–343. depositional setting of the coarse-grained Upper Cambrian Driscoll, J. P., Hall, M. and Mahmud, S. A. (2013) Applying Owen Conglomerate, West Coast Range, western Tasma- sedimentological techniques to document Cambrian- nia. Aust. J. Earth Sci. 50, 835–852. Ordovician rift basin evolution—northern and western Tas- Noll, C. A. and Hall, M. (2005) Structural architecture of the mania, Australia. Abstract: 30th IAS Meeting on Owen Conglomerate, West Coast Range, western Tasma- Sedimentology, Manchester, U.K., Id: T5S2. nia; field evidence for Late Cambrian extension. Aust. J. Gao, S. and Wedepohl, K. H. (1995) The negative Eu anomaly Earth Sci. 52, 411–426. in Archean sedimentary rocks: Implications for deposition, Noll, C. A. and Hall, M. (2006) Normal fault growth and its age and importance of their granitic sources. Earth Planet. function on the control of sedimentation during basin for- Sci. Lett. 133, 81–94. mation; a case study from field exposures of the Upper Garcia, D., Coehlo, J. and Perrin, M. (1991) Fractionation be- Cambrian Owen Conglomerate, West Coast Range, west-

tween TiO2 and Zr as a measure of sorting within shale and ern Tasmania, Australia. AAPG Bull. 90, 1609–1630. sandstone series (northern Portugal). Eur. J. Miner. 3, 401– Officer, G. L. and Hogg, E. G. (1895) Geological notes: Strahan 414. to Lake St Clair. Proc. Royal Soc. Vic. 7, 120 pp. Gu, X., Liu, J., Zheng, M., Tang, J. and Qi, L. (2002) Prov- Parisi, S., Paternoster, M., Perri, F. and Mongelli, G. (2011) enance and tectonic setting of the Proterozoic turbidites in Source and mobility of minor and trace elements in a vol- Hunan, South China: geochemical evidence. J. Sed. Res. canic aquifer system: Mt. Vulture (southern Italy). J. 72, 393–407. Geochem. Explor. 110, 233–244. Herron, M. M. (1988) Geochemical classification of terrigenous Perkins, C. and Walshe, J. L. (1993) Geochronology of the

Geochemistry of Owen Group Siliciclastics, Tasmania, Australia 209 Mount Read Volcanics, Tasmania, Australia. Econ. Geol. Robinson, P. (2003) XRF analysis of flux-fused discs. 88, 1176–1197. Geoanalysis 2003, Abstracts. Proc. The 5th International Perri, F. (2014) Composition, provenance and source weather- Conference on the Analysis of Geological and Environmen- ing of Mesozoic sandstones from Western-Central Medi- tal Materials, 90. terranean Alpine Chains. J. Afr. Earth Sci. 91, 32–43. Roser, B., Cooper, R., Nathan, S. and Tulloch, A. (1996) Re- Perri, F. and Ohta, T. (2014) Paleoclimatic conditions and connaissance sandstone geochemistry, provenance, and tec- paleoweathering processes on Mesozoic continental redbeds tonic setting of the lower Paleozoic terranes of the West from Western-Central Mediterranean Alpine Chains. Coast and Nelson, New Zealand. New Zealand J. Geol. Palaeogeogr. Palaeoclimatol. Palaeoecol. 395, 144–157. Geophys. 39, 1–16. Perri, F., Critelli, S., Mongelli, G. and Cullers, R. L. (2011a) Roser, B. P. and Korsch, R. J. (1986) Determination of tectonic

Sedimentary evolution of the Mesozoic continental redbeds setting of sandstone-mudstone suites using SiO2 content and using geochemical and mineralogical tools: the case of K2O/Na2O ratio. J. Geol. 94, 635–650. Upper Triassic to Lowermost Jurassic Monte di Gioiosa Ross, J. R. P. and Ross, C. A. (2007) Ordovician Bryozoans mudstones (Sicily, southern Italy). Int. J. Earth Sci. (Geol. and Sequence Stratigraphy in Tasmania. Assoc. Aust. Palae., Rundsch) 100, 1569–1587. 197–226. Perri, F., Muto, F. and Belviso, C. (2011b) Links between com- Sahraeyan, M. and Bahrami, M. (2012) Geochemistry of position and provenance of Mesozoic siliciclastic sediments sandstones from the Aghajari Formation, Folded Zagros from Western Calabria (Southern Italy). Ital. J. Geosci. 130, Zone, southwestern Iran: implication for paleoweathering 318–329. condition, provenance, and tectonic setting. Intl. J. Basic Perri, F., Critelli, S., Cavalcante, F., Mongelli, G., Dominici, Appl. Sci. 1, 390–407. R., Sonnino, M. and De Rosa, R. (2012a) Provenance sig- Seymour, D. B., Green, G. R. and Calver, C. R. (2007) The natures for the Miocene volcaniclastic succession of the Geology and Mineral Deposits of Tasmania. Geol. Sur. Bull. Tufiti di Tusa Formation, southern Apennines, Italy. Geol. 72. Mag. 149, 423–442. Slack, J. F. and Stevens, B. P. (1994) Clastic metasediments of Perri, F., Critelli, S., Dominici, R., Muto, F., Tripodi, V. and the Early Proterozoic Broken Hill Group, New South Wales, Ceramicola, S. (2012b) Provenance and accommodation Australia: Geochemistry, provenance, and metallogenic sig- pathways of late Quaternary sediments in the deep-water nificance. Geochim. Cosmochim. Acta 58, 3633–3652. northern Ionian Basin, southern Italy. Sed. Geol. 280, 244– Suttner, L. J. and Dutta, P. K. (1986) Alluvial sandstone com- 259. position and paleoclimate, Framework mineralogy. J. Sed. Perri, F., Critelli, S., Martín-Algarra, A., Martín-Martín, M., Res. 56. Perrone, V., Mongelli, G. and Zattin, M. (2013) Triassic Taylor, S. R. and McLennan, S. M. (1995) The geochemical redbeds in the Malaguide Complex (Betic Cordillera - evolution of the continental crust. Rev. Geophys. 33, 241– Spain): petrography, geochemistry, and geodynamic impli- 265. cations. Earth-Sci. Rev. 117, 1–28. Tribovillard, N., Algeo, T. J., Lyons, T. and Riboulleau, A. Perri, F., Dominici, R. and Critelli, S. (2015a) Stratigraphy, (2006) Trace metals as paleoredox and paleoproductivity composition and provenance of argillaceous marls from the proxies: an update. Chem. Geol. 232, 12–32. Calcare di Base Formation, Rossano Basin (northeastern von Eynatten, H., Barcela-Vidal, C. and Pawlowsky-Glahn, V. Calabria). Geol. Mag. 152, 193–209. (2003) Composition and discrimination of sandstones: a Perri, F., Critelli, S., Dominici, R., Muto, F. and Ponte, M. statistical evaluation of different analytical methods. J. Sed. (2015b) Sourceland controls and dispersal pathways of Res. 73, 47–57. Holocene muds from boreholes of the Ionian Basin, Calab- Wade, M. L. and Solomon, M. (1958) Geology of the Mt. Lyell ria, southern Italy. Geol. Mag. (in press). Mines, Tasmania. Econ. Geol. 53, 367–416. Perri, F., Caracciolo, L., Cavalcante, F., Corrado, S., Critelli, Watson, J. S. (1996) Fast, simple method of powder pellet prepa- S., Muto, F. and Dominici, R. (2015c) Sedimentary and ther- ration for X-ray fluorescence analysis. X-Ray Spectrometry mal evolution of the Eocene-Oligocene mudrocks from the 25, 173–174. southwestern Thrace Basin (NE Greece). Basin Res. (in Weissert, H., Joachimski, M. and Sarnthein, M. (2008) press). Chemostratigraphy. Newsletters Strati. 42, 145–179. Pettijohn, F. J. (1987) Sand and Sandstone. Springer, 553 pp. Yanjing, C. and Yongchao, Z. (1997) Geochemical characteris- Rahman, M. J. J. and Suzuki, S. (2007) Geochemistry of tics and evolution of REE in the early Precambrian sandstones from the Miocene Surma Group, Bengal Basin, sediments: Evidence from the southern margin of the North Bangladesh: Implications for Provenance, tectonic setting China craton. Episodes, 20, 109–116. and weathering. Geochem. J. 41, 415–428.

210 S. A. Mahmud et al.