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Magnetostratigraphic Chronology of a Cenozoic Sequence from DSDP

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Magnetostratigraphic Chronology of a Cenozoic Sequence from DSDP ORIGINAL RESEARCH published: XX 2020 doi: 10.3389/feart.2020.563453 1 58 2 59 3 60 4 61 5 62 6 63 7 64 8 Magnetostratigraphic Chronology of a 65 9 66 10 Cenozoic Sequence From DSDP Site 67 11 68 12 274, Ross Sea, Antarctica 69 13 70 14 Luigi Jovane 1*, Fabio Florindo 1,2,3,GaryWilson 4,5,Stephaniede Almeida Pecchiai Saldanha Leone 1, 71 15 Muhammad Bin Hassan 1,DanielRodelli 1 and Giuseppe Cortese 4 72 16 73 17 1Instituto Oceanográfico, Universidade de São Paulo, São Paulo, Brazil, 2Istituto Nazionale di Geofisica e Vulcanologia, Rome, 74 3 4 5 18 Italy, Institute for Climate Change Solutions, Pesaro e Urbino, Italy, GNS Science, Lower Hutt, New Zealand, Department of 75 Geology and Marine Science, University of Otago, Dunedin, New Zealand 19 76 20 77 21 New paleomagnetic results from the late Eocene-Middle Miocene samples from Deep Sea 78 22 Drilling Project Site 274, cored during Leg 28 on the continental rise off Victoria Land, Ross 79 23 Sea, provide a chronostratigraphic framework for an existing paleoclimate archive during a 80 24 81 25 key period of Antarctic climate and ice sheet evolution. Based on this new age model, the 82 26 cored late Eocene-Middle Miocene sequence covers an interval of almost 20 Myr (from 83 27 ∼35 to ∼15 Ma). Biostratigraphic constraints allow a number of possible correlations with 84 28 85 Edited by: the Geomagnetic Polarity Time Scale. Regardless of correlation, average interval sediment 29 86 Hagay Amit, accumulation rates above 260 mbsf are ∼6 cm/kyr with the record punctuated by a 30 87 Université de Nantes, France number of unconformities. Below 260 mbsf (across the Eocene/Oligocene boundary) 31 Reviewed by: 88 interval, sedimentation accumulation rates are closer to ∼1 cm/kyr. A major unconformity 32 Belén Oliva-Urcia, 89 33 Autonomous University of Madrid, identified at ∼180 mbsf represents at least 9 Myr accounting for the late Oligocene and 90 34 Spain Early Miocene and represent non-deposition and/or erosion due to intensification of 91 35 Chenglong Deng, 92 Antarctic Circumpolar Current activity. Significant fluctuations in grain size and 36 Chinese Academy of Sciences (CAS), 93 37 China magnetic properties observed above the unconformity at 180 mbsf, in the Early 94 38 *Correspondence: Miocene portion of this sedimentary record, reflect cyclical behavior in glacial advance 95 39 Luigi Jovane and retreat from the continent. Similar glacial cyclicity has already been identified in other 96 [email protected] 40 Miocene sequences recovered in drill cores from the Antarctic margin. 97 41 98 Specialty section: 42 Keywords: magnetostratigraphy, grain size, Ross Sea Antarctica, circumpolar current, Oligocene-Early Miocene 99 43 This article was submitted to 100 Geomagnetism and Paleomagnetism, 44 a section of the journal 101 45 Frontiers in Earth Science INTRODUCTION 102 46 103 Received: 18 May 2020 47 Accepted: 13 November 2020 Deep Sea Drilling Program (DSDP) Leg 28 (Figure 1) was designed to explore the long-term climatic, 104 48 Published: XX 2020 biostratigraphic and geological history of Antarctica and its environments (Hayes and Frakes, 1975). 105 49 Citation: Such geological records provide insights into modern and future climate sensitivity estimates, 106 50 Jovane L, Florindo F, Wilson G, de particularly for time periods characterized by the presence of continental ice sheets and a 107 51 Almeida Pecchiai Saldanha Leone S, paleogeography similar to modern (e.g., Markwick, 2007; Farnsworth et al., 2019). 108 52 Hassan MB, Rodelli D and Cortese G Earth’s climate underwent a stepwise shift from greenhouse to icehouse conditions during the 109 53 (2020) Magnetostratigraphic Cenozoic. Major ice sheets first appeared on Antarctica across the Eocene/Oligocene boundary co- 110 Chronology of a Cenozoic Sequence 54 incident with the earliest Oligocene Oi-1 oxygen isotope event (1.0‰ δ18O increase at ca. 33.55 Ma; 111 55 From DSDP Site 274, Ross 112 Sea, Antarctica. e.g., Miller et al., 1991; Zachos et al., 1996; Zachos et al., 2001; Miller, 2005a; Miller et al., 2005b; 56 Front. Earth Sci. 8:563453. Francis et al., 2009; Lurcock and Florindo, 2017, Westerhold et al., 2020). While long thought to be 113 57 doi: 10.3389/feart.2020.563453 associated with the early glaciation of Antarctica (Kennett, 1977), the Antarctic Circumpolar Current 114 Frontiers in Earth Science | www.frontiersin.org 1 November 2020 | Volume 8 | Article 563453 Jovane et al. Magnetostratigraphy of DSDP Site 274 115 172 116 173 117 174 118 175 119 176 120 177 121 178 122 179 123 180 124 181 125 182 126 183 127 184 128 185 129 186 130 187 131 188 132 189 133 190 134 191 135 192 136 193 137 194 138 195 139 196 140 197 141 198 142 199 143 200 144 201 145 202 146 203 147 204 148 205 149 FIGURE 1 | Map of Ross Sea with schematic representation of present-day Antarctic Slope Current (dashed white line) and the continental shelf current flow 206 (orange lines) (Ainley and Jacobs, 1981; Whitworth et al., 1995; Orsi and Wiederwohl, 2009). Location of DSDP Site 274 is indicated by a red star. DSDP 270, AND-2A, 150 Eltanin 27–21 and CRP are also shown because they are reference cores in the area (respectively, Kulhanek et al., 2019, Jovane et al., 2019; Jovane et al., 2008; Roberts 207 151 et al., 2013). 208 152 209 153 210 did not appear until the Late Oligocene (Lyle, et al., 2007). Oligocene, however, the cooling during the Miocene was not 154 211 Throughout the Oligocene, Antarctic ice sheets experienced monotonic, but characterized by swings between cooler and 155 212 repeated cycles of advance and retreat, as indicated by large warmer climate (e.g., Miller et al., 1991; Zachos et al., 1997; 156 213 and rapid changes in global sea level (Kominz and Pekar, Zachos et al., 2001; Lear et al., 2004; Holbourn et al., 2005; 157 214 2001) and δ18O variations in deep-ocean sediment (Pälike Shevenell et al., 2008; Holbourn et al., 2013; Holbourn et al., 158 215 et al., 2006). Following the inception of the Antarctic 2014; Holbourn et al., 2015; Lear et al., 2015; Holbourn et al., 2018; 159 216 Circumpolar Current, the Oligocene terminated with another Liebrand et al., 2017; Westerhold et al., 2020). 160 217 transient global cooling event (Mi-1, at ca. 23 Ma), After the initial onset of and recovery from Mi-1, the Early 161 218 characterized by a ∼1‰ positive excursion in marine benthic Miocene experienced relatively warm intervals. The warming 162 219 foraminiferal δ18O records (e.g., Wilson et al., 2009; Beddow et al., cycles of the Early Miocene culminated in the Mid-Miocene 163 220 2016) and associated with a large-scale Antarctic ice sheet Climatic Optimum (MMCO) at around 17–14 Ma, 164 221 expansion at the Oligocene-Miocene transition. This event was immediately followed by the Middle Miocene Climate 165 222 dramatic in scale, with the East Antarctic Ice Sheet (EAIS) Transition (MMCT) at 14.2–13.8 Ma (Shevenell et al., 2004). 166 223 estimated to have grown from 50 to 125% of its present-day The transition, as recorded in deep-ocean δ18O variations, was a 167 224 size (e.g., Pekar et al., 2006). It was the first of a series of similar significant one: the MMCO was the warmest interval since the 168 225 “Mi-” oxygen isotope events that, while less extreme than Mi-1, Eocene, while the MMCT, and the subsequent cooling during the 169 226 were responsible for the progressive cooling and glaciation rest of the Miocene, produced temperatures colder than any 170 227 experienced by Antarctica during the Miocene. As in the previously observed in the Cenozoic. During this time, there 171 228 Frontiers in Earth Science | www.frontiersin.org 2 November 2020 | Volume 8 | Article 563453 Jovane et al. Magnetostratigraphy of DSDP Site 274 229 was a sizable EAIS, as inferred from δ18O, sea level curves and de Astronomia, Geofísica e Cienciasˆ Atmosféricas da Universidade 286 230 direct sedimentological evidence from the Antarctic continent de São Paulo (IAG USP) in a magnetically shielded room using a 2 G 287 231 itself (e.g., Lewis et al., 2007). Enterprises magnetometer (Model 755–4K). Grain size, magnetic 288 232 In this paper, we present the first magnetostratigraphic susceptibility and rock magnetic analyses were conducted at the 289 233 chronology of a late Eocene-Early Miocene record from a Centro Oceanográfico de Registros Estratigráficos (CORE) at the 290 234 sediment core (DSDP Leg 28, Site 274) obtained from offshore Instituto Oceanográfico da Universidade de São Paulo (IO USP) 291 235 Cape Adare in the Ross Sea Sector of the Antarctic continent in using a Microtrac Bluewave-SIA, an AGICO MFK1-FA 292 236 1973. The new age model will allow further studies of this unique Kappabridge, and a Vibrating Sample Magnetometer (VSM) 293 237 core to produce future paleoenvironmental reconstructions MicroMag 3,900 Princeton-Lake Shore Cryotronics, respectively. 294 238 focusing on the discharge of sediments from the catchment 295 239 areas in this region of the Ross Sea (e.g., Sagnotti, et al., 1998; 296 240 Grain Size 297 Jovane et al., 2004; Jovane et al., 2019; Roberts et al., 2013). Samples were prepared by crushing ∼0.2 g of bulk sediment in an 241 298 agate mortar. The crushed samples were further disaggregated 242 299 using 10% hydrogen peroxide to remove organic matter. After 243 300 SITE LOCATION AND LITHOLOGY 48 h of reaction, the samples were passed through 2 mm sieves 244 301 and dried in an oven.
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