advances.sciencemag.org/cgi/content/full/3/5/e1602567/DC1

Supplementary Materials for

Australian shelf sediments reveal shifts in Miocene

Southern Hemisphere westerlies

Jeroen Groeneveld, Jorijntje Henderiks, Willem Renema, Cecilia M. McHugh, David De Vleeschouwer,

Beth A. Christensen, Craig S. Fulthorpe, Lars Reuning, Stephen J. Gallagher, Kara Bogus,

Gerald Auer, Takeshige Ishiwa; Expedition 356 Scientists

Published 10 May 2017, Sci. Adv. 3, e1602567 (2017)

DOI: 10.1126/sciadv.1602567

This PDF file includes:

Expedition 356 Scientists

Supplementary Text

fig. S1. Lithostratigraphic column for IODP Site U1464, including recovery,

biostratigraphic tie points, interpreted facies, K (%), Th/K versus sediment depth,

and photos of sabhka and dolostone facies.

fig. S2. Lithostratigraphic column for IODP Site U1459 including recovery,

biostratigraphic tie points, K (%), and Th/K versus sediment depth.

fig. S3. Correlation of the K-record with K-feldspar obtained from bulk

mineralogy XRD analyses plotted versus depth, and as scatter plot.

fig. S4. T-F WFFT of the K-records from sites U1459 and U1464 along their

respective biostratigraphic age model, and age versus sediment depth.

fig. S5. T-F WFFT of the K-records from Sites U1459 and U1464 versus ETP

solution (39, 42), and in comparison with those performed on the benthic 18O

records from ODP Site 1146 in the South China Sea (40) and ODP Site 1085 in

the South Atlantic (41) for the same time interval.

table S1. Biostratigraphic datums used for the biostratigraphic age model.

table S2. Paired potassium feldspar (%), quartz (%, only shipboard; n.d., no data),

and K-log (%) results versus depth in core for Site U1459.

References (43–48)

Expedition 356 Scientists: D. C. Potts12, T. Himmler1, M. A. Kominz13, C. A. Korpanty14, B.

L. Mamo15, H. V. McGregor16, S. Baranwal17, I. S. Castañeda18, D. R. Franco19, M. Gurnis20,

C. Haller21, Y. He22, H. Iwatani15, R. S. Jatiningrum23, E. Y. Lee24, E. Levin25, B. F. Petrick26,

A. Rastigar27, H. Takayanagi28, W. Zhang29.

12Ecology & Evolutionary Biology and Institute of Marine Sciences, University of California, Santa Cruz, 1156 High Street,

Santa Cruz, CA 95064, USA. 13Department of Geosciences, Western Michigan University, 1903 West Michigan Ave., 1187

Rood Hall, Kalamazoo, MI 49008, USA. 14School of Biological Sciences, University of Queensland, Level 8, Gehrmann

Bldg., Brisbane 4072, Australia. 15School of Biological Sciences, The University of Hong Kong, Kadoorie Biological

Sciences Building, Pokfulam Road, Hong Kong SAR, China. 16School of Earth and Environmental Sciences, University of

Wollongong, Northfields Avenue, Wollongong NSW 2522, Australia. 17Geological Survey of Norway, Leiv Eirikssons vei

39, Trondheim 7040, Norway, and CAGE - Centre for Arctic Gas hydrate, Environment and climate, UiT, Postboks 6050

Langnes, N-9037 Tromsø, Norway. 18Department of Geosciences, University of Massachusetts, 611 N. Pleasant St., 233

Morrill Science Center II, Amherst, MA 01003, USA. 19Department of Geophysics, National Observatory, Rua Gal. Jose

Cristino, 77, Rio de Janeiro RJ 20921-400, Brazil. 20Division of Geological and Planetary Sciences, California Institute of

Technology, 1200 East California Blvd., MC 2520-21, Pasadena, CA 91125, USA. 21College of Marine Science, University

of South Florida, 140 7th Ave. South, St. Petersburg, FL 33701, USA. 22Earth Sciences, Zhejiang University, 38 Zheda Road,

Hangzhou Zhejiang, P.R. China. 23Geoscience, Geotechnology and Material Resource Engineering, Akita University, 1-1

Gakuen-cho, Tegata, Akita-shi 010-8502, Japan. 24Department of Geodynamics and Sedimentology, University of Vienna,

UZA II Althanstrasse 14, Vienna 1090, Austria. 25Department of Earth and Planetary Sciences, University of California,

Davis, CA 95616, USA. 26School of Geography, Politics & Sociology, University of Newcastle Upon Tyne, Daysh Bldg,

Newcastle upon Tyne NE1 7RU, United Kingdom. 27School of Applied Geology, Curtin University, PO Box 315, Mounty

Hawthorn WA 6915, Australia. 28Institute of Geology and Paleontology, Tohoku University, Aobayama, Sendai 980-8578,

Japan. 29MOE Key Laboratory of Surficial Geochemistry, Department of Earth Sciences, Nanjing University,163

Xianlindadao Road Nanjing 210046, P.R. China.

Supplementary Text

Potassium (K) and Thorium/Potassium (Th/K) as proxies for siliciclastic input

The K-component of NGR logs provides information on the concentration of

aluminosiliciclastic input. In marine sediments, K mainly derives from K-feldspar (43) or

illite (44), which are preferentially transported fluvially as fine-grained material (14, 15).

XRD analysis of bulk mineralogy at Site U1459 shows that K-feldspars are the dominant K-

bearing minerals, while the content of clay minerals (e.g., illite) is below or close to the

detection limit. The K-feldspars are also correlated with the quartz content (R2=0.76) and the

abundance of both minerals co-varies with the NGR-derived K-record (fig. S3). The

interpretation of K(%) could be hampered by dilution of K in the sediment. Variations in

carbonate content are the main source of variation such that potentially changes in siliciclastic

supply can be masked, especially on shorter timescales. In the current study, however, we

only present long-term changes in K(%) during which the carbonate content does not vary

significantly (12). We therefore interpret high K values as indicators for fluvial activity

providing evidence for continental moisture. Thorium commonly occurs in aluminosilicates

similar to K, but is also enriched in heavy minerals (45-47), which are concentrated in larger

eolian particles delivered off Western Australia (16). Previous studies have used the relative

abundance of fluvial and eolian-related elements to reconstruct variations in precipitation and

aridity off the coast of Western Australia over the last 500 kyr (16), and since the Last Glacial

Maximum (15). These studies showed strong variations on glacial-interglacial timescales

between both components, demonstrating that the reconstruction of fluvial versus eolian

sediment input is a powerful tool to reconstruct past climate conditions for Western Australia.

We use the ratio between Th and K to provide an estimation of relative moisture/aridity

independent from dilution impacts. When conditions become wetter, the influx of K via rivers

increases and Th related to heavy mineral supply via dust decreases. We tentatively define dry

conditions when Th/K>20 and K<0.2%, wet conditions when Th/K<10 and K>0.3%, and

intermediate conditions by K values between 0.2 and 0.3% (Fig. 3, S2–S3) (48).

Shipboard XRD analysis of one sample from the Miocene section at Site U1464 confirms that

K-feldspar, clay minerals and quartz are only present in trace amounts (~1%) in the interval

with low K-log values.

Lithostratigraphy of IODP sites U1464 and U1459

At Site U1464, which is the northernmost site in the Expedition 356 transect, the middle to

late Miocene lithology primarily consists of mud (mudstone, wackestone) and grain

(packstone, grainstone) supported dolomitic limestone and dolostone (fig. S1). The

sedimentary structures and mineralogy contained in these sediments reveal an arid and

dynamically changing environment from neritic to supratidal (16–14 Ma) to sabkha, with

evidence for pronounced evaporative (14.1–12.6 Ma) to shallow subtidal (12.6–6.25 Ma)

conditions. Throughout the Miocene section there is evidence for shallow water and

evaporative conditions manifested by the occurrence of anhydrite nodules with chicken wire

texture, gypsum nodules, dissolution features, and tidal structures such as parallel laminae

(fig. S1). The most pronounced evaporative facies, similar to present-day sabkha, occurs from

14.1–12.6 Ma (625–525 m WMSF) (fig. S1). In this interval, anhydrite is found in nodules,

up to 10 cm in length, infilling burrows and possible dessication features (mud cracks). Dark

brown intervals, up to one meter thick, of parallel laminae in which growing anhydrite

nodules have displaced the sediment, are particularly common in the dolostone. Other well-

preserved sedimentary features typical of supratidal settings include load casts and ball-and-

pillow structures. The absence of bioclasts and the lack of bioturbation suggest that the

environment in these darker intervals was not conducive to biological activity. The most

intense evaporative conditions are linked to prominent depositional events, a few centimeters

thick: black, organic-rich, carbonate-poor dolostone, suggestive of subaerial exposure (fig.

S1).

In contrast to northern Site U1464, the southern Site U1459 contains grain-supported

(packstone and grainstone) dolomitic limestones interbedded with quartz-rich sandstone

intervals (fig. S2). Site U1459 was located in deeper waters, possibly a middle to outer shelf

setting. The benthic foraminifera fauna had low diversity, with assemblages typical of outer

shelf settings (e.g., Cibicidoides spp., Fonbotia wuellerstorfi, Heterolepa sp., Melonis spp.),

consistent with the percentage planktonic foraminifera of 30–65%. Increasing K values in the

logs correspond to lithological intervals rich in quartz and K-feldspar sand, which are linked

to river outflow (figs. S1, S2). The overall sedimentological trend from 12–8 Ma is one of

increasingly wetter conditions likely associated with stronger fluvial input. K-feldspar and

quartz decrease in the muddier sections and so do the K values representing periods of

slightly less fluvial input (figs. S1, S2). The correlation between wet periods and the K-record

is well supported by these observations.

fig. S1. Lithostratigraphic column for IODP Site U1464, including recovery,

biostratigraphic tie points, interpreted facies, K (%), Th/K versus sediment depth, and

photos of sabhka and dolostone facies. (A) Lithostratigraphic column for IODP Site U1464

including recovery, biostratigraphic tie points, interpreted facies, K (%) and Th/K versus

sediment depth. Blue (and higher values) and green bar indicate the range of values for

dominantly wet conditions. See (B) and (C) on next page.

fig. S1. (continued): (B) Sabkha facies with anhydrite nodules displacing dolostone from Site

U1464 (Core 356-U1464C-25R). Depths are centimeters within the core section. (C) Tidal

flat dolostone with intertidal laminations and anhydrite from Site U1464 (Core 356-U1464C-

25R). Depths are centimeters within the core section.

fig. S2. Lithostratigraphic column for IODP Site U1459 including recovery,

biostratigraphic tie points, K (%), and Th/K versus sediment depth. Blue (and higher

values) and green bar indicate the range of values for dominantly wet conditions. Shipboard

XRD analyses for K-feldspar and quartz are shown along with the K-record.

fig. S3. Correlation of the K-record with K-feldspar obtained from bulk mineralogy

XRD analyses plotted versus depth, and as scatter plot. (A) Correlation of the K-record (9

pt running average) with K-feldspar obtained from bulk mineralogy XRD analyses plotted

versus depth from the mid to late Miocene. Poor core recovery prevented more closely spaced

samples in the lower 50 m. (B) Scatter plot between the K values and K-feldspar suggesting a

statistically significant relationship. Accordingly, the K-record can be interpreted as a proxy

for fluvial transport and, thus, increased moisture in the source area.

fig. S4. T-F WFFT of the K-records from sites U1459 and U1464 along their respective

biostratigraphic age model, and age versus sediment depth. (A) Time-Frequency

Weighted Fast Fourier Transform of the K-records from sites U1459 and U1464 along their

respective biostratigraphic age model. Underestimated sedimentation rates in the older portion

of U1459 have been corrected by astronomical calibration of 405 kyr eccentricity cycles. See

(B) on next page.

1 0.8 0.6 0.4 0.2 0

K (%)

22

20

18

16

14

12

10

8

6

Age

(M

a)

Sed

imen

tatio

n r

ate

undere

stim

ate

d

by b

iostr

atig

raphic

age m

od

el

0.4 0.2 0

K (%)

100-

kyr

405-

kyr

100-

kyr

405-

kyr

bandpass

300-500 kyr

bandpass

300-500 kyr

Site U1459 Site U1464

bandpass 500-1000 kyr

0 0.005 0.01

Frequency (1/kyr)

0 0.005 0.010.015

Frequency (1/kyr)

22

20

18

16

14

12

10

8

6

fig. S4. (continued): (B) Age versus sediment depth (m WMSF) for sites U1459 and U1464.

Biostratigraphic markers are indicated by blue stars; black line represents the age model based

on biostratigraphic datums; red line represents age model after cyclostratigraphic tuning was

performed.

0.7

50

.50

.25

0

K (

%)

0.5

0.2

50

K (

%)

100-

kyr

405-

kyr

41-k

yr

84

0-4

ET

P

17

16

15

14

13

12

11

109876

Age (Ma)

100-

kyr

405-

kyr

41-k

yr

fre

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(1/k

yr)

fre

qu

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(1/k

yr)

fre

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(1/k

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(‰

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3.5

32

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(‰

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(1/k

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(1/k

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Site U

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Site

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100-

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405-

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41-k

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00

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00

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0.0

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00

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100-

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405-

kyr

fig. S5. T-F WFFT of the K-records from Sites U1459 and U1464 versus ETP solution

(39, 42), and in comparison with those performed on the benthic 18O records from ODP

Site 1146 in the South China Sea (40) and ODP Site 1085 in the South Atlantic (41) for

the same time interval.

table S1. Biostratigraphic datums used for the biostratigraphic age model. Cored depth

scale (m CSF-A) was converted to wireline matched below sea floor depth (m WMSF) to

construct age-depth models for the log data presented herein. CN = calcareous nannofossils;

LBF = larger benthic foraminifera. *=Maximal age; possibly younger than its stratigraphic

base.

Depth CSF-A (m)

Depth WMSF (m)

Biostratigraphic Event Type Age (Ma)

Reference

U1459

165.26 171.66 Top D. quinqueramus CN 5.59 Gradstein et al., 2012

209.84 214.63 Base D. brouweri CN 10.76 Gradstein et al., 2012

223.9 228.21 Top Cy. floridanus CN 11.85 Gradstein et al., 2012

243.9 247.51 Base R. pseudoumbilicus CN 12.83 Gradstein et al., 2012

278.47 279.98 Presence R. haqii CN 22.82* Young, 1998

U1464

281.39 281.00 Top D. quinqueramus CN 5.59 Gradstein et al., 2012

312.75 312.44 Top R. rotaria CN 6.25 Young, 1998

453.5 453.56 Top Flosculinella LBF 11.60 Renema et al., 2015;

Allan et al., 2000

579.91 580.29 above Base C. macintyrei CN 13.36 Gradstein et al., 2012

745.0 746.31 Base N. ferreroi LBF 16 Renema, 2007;

Marshall et al., 2015

table S2. Paired potassium feldspar (%), quartz (%, only shipboard; n.d., no data), and

K-log (%) results versus depth in core for Site U1459. Results marked with an asterix (*)

are shipboard results.

Depth WMSF (m) K-spar (%) Quartz (%) K-log (%)

167.19 14.21 n.d. 0.4759

167.65 16.61 n.d. 0.5675

168.25 16.26 n.d. 0.5483

169.12 16.05 n.d. 0.5179

169.48 15.27 n.d. 0.4572

170.55 15.93 n.d. 0.5747

170.95 19.53 n.d. 0.5880

171.71 17.80 n.d. 0.4471

171.81 14.68 n.d. 0.4622

172.37 13.66 n.d. 0.3590

172.77 10.31 n.d. 0.3824

173.17 17.22 n.d. 0.4042

173.64 13.58 n.d. 0.3720

174.6 17.06 n.d. 0.3640

175 15.94 n.d. 0.2841

175.66 14.65 n.d. 0.2603

176.23 9.49 n.d. 0.3171

176.73 10.22 n.d. 0.2469

177.29 15.93 n.d. 0.3074

177.69 9.89 n.d. 0.1980

178.56 20.32 n.d. 0.2455

178.76 13.98 n.d. 0.2107

179.12 22.66 n.d. 0.2896

180.78 11.01 n.d. 0.2499

181.25 8.95 n.d. 0.2730

182.21 16.94 n.d. 0.2923

183.28 14.34 n.d. 0.5459

183.68 11.58 n.d. 0.7320

184.04 15.19 n.d. 0.6451

184.84 10.93 n.d. 0.5270

185.3 23.05 n.d. 0.6922

185.4 10.32 n.d. 0.6893

185.77* 8.4 9.7 0.8570

186.37 15.37 n.d. 0.6582

186.77 15.54 n.d. 0.5566

187.23 12.29 n.d. 0.5330

187.8 18.43 n.d. 0.6116

188.2 15.60 n.d. 0.7830

189.26 17.09 n.d. 0.7100

189.82 24.51 n.d. 0.6071

190.88* 3.5 3.9 0.5571

191.29 22.39 n.d. 0.5408

191.75 19.26 n.d. 0.4824

192.25 15.68 n.d. 0.3803

194.38 17.25 n.d. 0.4720

195.04 16.38 n.d. 0.4754

195.35 14.90 n.d. 0.3838

195.82 22.68 n.d. 0.3252

200.33 11.02 n.d. 0.3644

200.83 11.53 n.d. 0.2825

201.89 14.00 n.d. 0.4251

202.19 25.46 n.d. 0.4861

202.86 16.82 n.d. 0.5560

203.52 17.43 n.d. 0.4986

203.92 19.57 n.d. 0.4064

205.01 21.73 n.d. 0.3945

205.48 14.00 n.d. 0.3798

208.47 8.95 n.d. 0.1766

209.43 9.47 n.d. 0.2181

212.49 13.50 n.d. 0.3925

212.79 19.84 n.d. 0.4197

213.06 15.64 n.d. 0.3368

214.53 20.47 n.d. 0.4020

214.78 19.36 n.d. 0.4786

215.25 19.36 n.d. 0.3628

219.92 10.04 n.d. 0.0766

220.23 12.21 n.d. 0.0906

221.55 11.99 n.d. 0.1681

222.05 11.46 n.d. 0.1890

222.67 6.23 n.d. 0.1754

224.38 17.32 n.d. 0.2959

224.39* 15.2 9.3 0.2990

238.08* 12.2 7.5 0.0102

247.35 8.26 n.d. 0.0655

247.38* 3.0 4.7 0.0655

252.29 12.00 n.d. 0.2068

252.32 10.63 n.d. 0.2086

252.34 7.02 n.d. 0.2097

252.58 6.96 n.d. 0.2163

256.83 16.23 n.d. 0.2794

260.83 10.47 n.d. 0.1312

266.1 8.56 n.d. 0.1054

267.39 5.72 n.d. 0.1530

279.69* 0.9 0.2 0.1024

283.99* 0.9 0.0 0.2553