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Clay Mineral Assemblages in Hemipelagic Sediments Entering the Sumatra Subduction Zone, IODP Sites U1480 and U1481, Expedition 362

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Clay Mineral Assemblages in Hemipelagic Sediments Entering the Sumatra Subduction Zone, IODP Sites U1480 and U1481, Expedition 362 McNeill, L.C., Dugan, B., Petronotis, K.E., and the Expedition 362 Scientists Proceedings of the International Ocean Discovery Program Volume 362 publications.iodp.org https://doi.org/10.14379/iodp.proc.362.204.2020 Contents Data report: clay mineral assemblages 1 Abstract 1 Introduction in hemipelagic sediments entering the Sumatra 3 Methods 7 Results subduction zone, IODP Sites U1480 and U1481, 12 Conclusions 1 13 Acknowledgments Expedition 362 13 References Karissa Rosenberger,2 Michael B. Underwood,2 Peter Vrolijk,2 and Samuel Haines3 Keywords: International Ocean Discovery Program, IODP, JOIDES Resolution, Expedition 362, Sumatra Subduction Zone, Site U1480, Site U1481, Sunda-Sumatra subduction zone, X-ray diffraction, clay mineral assemblages, illite polytypes, illite crystallinity, illite-mica bo, smectite Abstract ducted to seismogenic depths in the northern Sumatran subduction zone, which is part of the 5000 km long Sunda subduction zone sys- This report documents the results of X-ray diffraction analyses tem (Figure F1). Regionally, the input materials of this subduction of 132 mud and mudstone samples collected offshore Sumatra zone are composed largely of trench-wedge and Bengal-Nicobar during International Ocean Discovery Program Expedition 362. Fan sediments with a total thickness of 4–5 km (McNeill et al., The clay-size mineral assemblage consists of smectite, illite, chlor- 2017b). Beneath the fan sediments is a basal pelagic interval that ite, kaolinite, and quartz. The relative abundance of smectite at Site overlies the basaltic crust of the subducting oceanic plate (Figure U1480 decreases downsection from a mean value of 33 wt% in Unit F2). Two sites (U1480 and U1481) were drilled, cored, and logged I to a mean of 19 wt% in Unit II; illite increases from a mean of 49 about 250 km southwest of the subduction front (Figure F1). wt% to a mean of 59 wt%. Smectite in Unit III increases to a mean of The primary drilling objective for Site U1480 was to recover a 73 wt%, and illite decreases to a mean of 19 wt%. Mean values are complete section of the incoming sedimentary section and upper- subordinate (<16 wt%) for undifferentiated chlorite + kaolinite and most basaltic basement (McNeill et al., 2017b). Six lithologic units <7 wt% for quartz in all units. A significant compositional discrep- were identified based on major changes in grain size, bed thickness, ancy occurs between Subunit IIIA at Site U1480 (mean smectite = and composition (McNeill et al., 2017a; McNeill et al., 2017b). Unit 64 wt%) and Unit III at Site U1481 (mean smectite = 36 wt%). At I (0–26.42 meters below seafloor [mbsf]) is early Pleistocene to Ho- Site U1480, the expandability of illite/smectite mixed-layer clays in- locene in age and composed of calcareous clay with interbeds of creases downsection, which is opposite to the trend expected with fine-grained sand, silty clay, and minor volcanic ash. Unit II (26.42– burial diagenesis. The maximum value is 88% within smectite-rich 1250.35 mbsf) is late Pliocene to early Miocene in age and contains samples from Unit III. Values of the illite crystallinity index are be- thin to medium beds of sandy silt and fine-grained sand (turbidites) tween 0.42Δ°2θ and 0.76Δ°2θ, with most data straddling the generic that transition downsection into claystone, silty claystone, and boundary between advanced diagenesis and anchimetamorphism. muddy sandstone. Unit III (1250.35–1327.23 mbsf) is late Paleo- Illite (060) reflections yield bo values of 8.988 to 9.000, which are in- cene to late Miocene in age and contains claystone and tuffaceous dicative of low phengite contents. Smectite (060) reflections display silty claystone. Unit IV (1327.23–1349.80 mbsf) is Late Cretaceous peak apex positions of 61.998°–61.798°2θ, which are consistent with to late Paleocene in age and contains basalt, tuffaceous and volcani- the mineral structure of montmorillonite. The detrital illite fraction clastic sandstone, and volcaniclastic breccia. Unit V (1349.80– contains 46%–60% 2M1 polytype, and the remainder is 1M/1Md. 1415.35 mbsf) is Late Cretaceous in age and contains calcareous claystone, chalk, and intercalated basalt intrusions. Unit VI Introduction (1415.35–1431.63 mbsf) is also late Cretaceous in age but com- posed entirely of basalt, which was interpreted to be the top of igne- International Ocean Discovery Program (IODP) Expedition 362 ous oceanic crust (McNeill et al., 2017a; McNeill et al., 2017b). focused on recovering the sedimentary section that will be sub- 1 Rosenberger, K., Underwood, M.B., Vrolijk, P., and Haines, S., 2020. Data report: clay mineral assemblages in hemipelagic sediments entering the Sumatra subduction zone, IODP Sites U1480 and U1481, Expedition 362. In McNeill, L.C., Dugan, B., Petronotis, K.E., and the Expedition 362 Scientists. Sumatra Subduction Zone. Proceedings of the International Ocean Discovery Program, 362: College Station, TX (International Ocean Discovery Program). https://doi.org/10.14379/iodp.proc.362.204.2020 2 Department of Earth and Environmental Science, New Mexico Institute of Mining and Technology, USA. Correspondence author: [email protected] 3 Nanyang Technological University, Singapore. MS 362-204: Received 17 February 2020 · Accepted 19 May 2020 · Published 13 July 2020 This work is distributed under the Creative Commons Attribution 4.0 International (CC BY 4.0) license. K. Rosenberger et al. Data report: clay mineral assemblages in hemipelagic sediments At Site U1481, the primary drilling objective was to core and log al., 2017a; McNeill et al., 2017b) were correlated with Units II and the deeper part of the stratigraphic section because it contains in- III at Site U1480 on the basis of age and lithology. Unit II (1149.70– tervals that may become the plate boundary décollement farther 1360.12 mbsf) is late Miocene in age and contains claystone, silty landward (McNeill et al., 2017b). Two lithologic units (McNeill et claystone, and muddy sandstone. Unit III (1360.12–1498.72 mbsf) is early to late Miocene in age and consists of claystone (McNeill et Figure F1. Map of eastern Indian Ocean showing locations of Sunda-Sumatra al., 2017a; McNeill et al., 2017b). subduction zone, Bengal and Nicobar Fans, and Sites U1480 and U1481. This report summarizes the results of X-ray diffraction (XRD) analyses of clay-size fractions from 132 core samples extracted from 20° N Sites U1480 and U1481. Samples were preferentially collected from India Bay of clay-rich intervals of the cores rather than interbeds of turbidites. Bengal 15° Most sample intervals in the split cores were positioned immedi- ately adjacent to whole-round specimens that were extracted for studies of interstitial water geochemistry and frictional-hydro- 10° geologic properties, and clay XRD specimens were co-located in “clusters” together with discrete specimens for bulk powder XRD, carbon-carbonate, grain-size analysis, and moisture and density; 5° U1480 additional samples were taken to document significant local litho- logy changes (e.g., transition from coarser grained to finer grained Bengal U1481 Sumatra 0° Fan intervals, decrease in carbonate content, or change in color) to en- sure both “representative” and end-member clay mineral composi- Nicobar tions. Our primary objective is to document changes in proportions Fan 5° of smectite, illite, chlorite + kaolinite, and quartz in mud and mud- S stone specimens relative to depth below seafloor and lithostrati- Sunda Trench e graphy. Such information can be used to infer how paleoclimate, 10° idg detrital provenance, and first-order patterns of sediment dispersal st R may have changed over time (e.g., Biscaye, 1965; Petschick et al., 15° 1996; Thiry, 2000; Gingele et al., 2001; Phillips et al., 2014). Such in- Ninetyea formation is relevant to the objectives of Expedition 362 because large variations in the proportions of clay minerals may have signif- 20° icant effects on frictional properties and dehydration reactions as 70°E 75° 80° 85° 90° 95° 100° 105° 110° Figure F2. Simplified composite of seismic reflection profiles showing locations of Sites U1480 and U1481 (from McNeill et al., 2017b). Blue line = interpreted unconformable boundary between Bengal-Nicobar Fan sediments and overlying trench wedge. Subduction zone SW deformation front U1480 NE 6 6 Nicobar Fan Trench wedge Ninetyeast 7 Ridge 7 Igneous crust 8 Two-way traveltime ( s) 8 20 km 9 9 NE Subduction zone 4 SW deformation front 5 5 U1481 6 6 Nicobar Fan Ninetyeast Trench wedge 7 Ridge 7 Igneous crust 8 8 Two-way traveltime9 ( s) 9 20 km 10 10 IODP Proceedings 2Volume 362 K. Rosenberger et al. Data report: clay mineral assemblages in hemipelagic sediments sedimentary strata enter the deeper subduction zone (e.g., Geersen Figure F3. Representative X-ray diffractograms for typical sample air-dried, et al., 2013; Hüpers et al., 2017). glycol saturated, and heated to 550°. Glycol saturation causes expansion of In addition to the basic mineral assemblages, we made measure- the smectite mineral structure and separates it from the chlorite (001) peak. ments intended to probe clay provenance and thermal maturity Note that intensities of chlorite (002) and (004) peaks are similar before and after heating, indicating little contribution from kaolinite. The increase in state, including evidence of the extent of smectite-to-illite dia- illite (001) peak intensity after heating is due to collapse of the smectite genesis, identification of specific varieties of smectite (dioctahedral (001) structure. versus trioctahedral), measurement and computation of bo values for the detrital illite assemblage, and determination of proportions Air-dried 4000 Illite (001) of 1M/1Md versus 2M1 polytypes in the detrital illite-mica assem- blages. In the context of our study, proportions of 2M1 versus Quartz (101) 1M/1Md polytypes yield information about the generic environ- Chlorite (002) mental conditions during illite formation in the prospective detrital 3000 kaolinite (001) source areas (e.g., Frey et al., 1983; Paudel and Arita, 2006).
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