SUPPLEMENTARY MATERIAL

GSA Data Repository 2020046

Coupled supercontinent-mantle plume events evidenced by

oceanic plume record

Luc S. Doucet1*, Zheng-Xiang Li1, Richard Ernst2,3, Uwe Kirscher1,4, Hamed Gamal El

Dien1,5, Ross N. Mitchell1,6

1Earth Geodynamic Research Group, TIGeR, School of Earth and Planetary Sciences, Curtin

University, Perth WA 6845, Australia, luc.serge.doucet@gmail.com

2 Department of Earth Sciences, Carleton University, Canada

3 Faculty of Geology and Geography, Tomsk State University, Russia

4Department of Geosciences, Eberhard Karls University Tübingen, Sigwartstr. 10, 72076 Tübingen, Germany 5Geology Department, Faculty of Science, Tanta University, 31527 Tanta, Egypt 6State Key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China

SUPPLEMENTARY MATERIAL

Lifespans of the known supercontinents

The names and lifespans of the supercontinents Pangea (ca. 320–170 Ma) and Rodinia (900–700

Ma) are discussed by Evans et al. (2016) and updated by Nordsvan et al. (2018) and Pourteau et

al. (2018) for Nuna (1600-1400 Ma). The supercontinents are defined by Meert (2012) as a

continued continental area that contain over 75% of landmass at a given age. As such,

Gondwana, with 60% of the global continental area, is not considered a true supercontinent but

part of processes that lead to the final assembly of the supercontinent Pangea. While the tenures

of supercontinents are fairly well constrained by paleomagnetic and geological data, the

assembly and breakup are protracted multistage processes marked by gradual shading on Figures

2 and 3.

Geological and geochemical evidence of plume-related material in ophiolite belts

Oceanic plume-related magmas are those of oceanic plateaus and ocean island basalts (OIB),

here we collected called O-LIPs. They are characterized by peculiar geological and geochemical

characteristics distinct from volcanic sequence of other tectonic settings as define by (Bryan and

Ernst, 2008; Dilek and Furnes, 2011; Kerr et al., 2000) (GSA Data Repository Table S1).

Names and ages of O-LIP occurrences in the database

The names of the oceanic mantle plume occurrences are the name of the locality where the

oceanic plateau, ocean island basalt or seamount has been described by the original authors (see

GSA Data Repository Table S2). In Table S2 we list the maximum and minimum ages as well as

the preferred age for magmatic emplacement reported by the authors. The magmatic ages are

used for Figures 2 and 3 and the time series analysis. All the references in are reported in the

GSA Data Repository Table S2 and below.

The continental LIP records

The C-LIP record in this study has been updated from the Large Igneous Provinces Commission

database and are presented in the GSA Data Repository Table S3. According to the Large

Igneous Provinces Commission (Ernst 2014), the C-LIP includes flood basalt provinces, dike

swarm and silicic large igneous province (SLIP). All the references in are reported in the GSA

Data Repository Table S3 and below.

Time series analyses

We conduct time series analysis on both the continental and oceanic LIP records (GSA Data

Repository Table S2 and S3) to test for the presence of any significant cycles or cyclic trends.

We applied a Fast-Fourier transform (FFT) (GSA Data Repository Figure S1 and S2) and a

multi-taper method (MTM) (GSA Data Repository Figure S3 and S4). For the FFT, the spectral

power used is the complex conjugate of the Fourier coefficients, normalized to unit mean power

(Muller and MacDonald, 2000). First, we evaluated the significance of the FFT spectral peaks

using a Monte Carlo routine to simulate white noise (Muller and MacDonald, 2000). FFTs were

performed on each of these 1000 randomly generated time series; a 95% and 90% confidence

level was typically approximated for each frequency by multiplying the mean power by three and

two respectively (Muller and MacDonald, 2000). We interpret spectral peaks rising above 90%

confidence level as statistically significant. Based on the FFT results, we ran bandpass filters

with Gaussian windows to encapsulate the significant peaks identified. Since we are dealing with

unevenly sampled and rather small datasets, the afore mentioned spectral analysis approach

might underestimate the true uncertainty especially for the long wavelength cycles. We

additionally applied a MTM on the datasets using red noise as a null hypothesis (Ghil et al.,

2002). The data were binned using window sizes of 10 Ma (O-LIP) and 29 Ma (C-LIP).

Furthermore, we used a linear interpolation to obtain an equally spaced dataset for usage for the

spectral analysis. To obtain the MTM results we use the SSA-MTM toolkit (Ghil et al., 2002).

We applied bandpass filters manually using as narrow windows as possible without

disappearance of the signal. Based on the SSA-MTM toolkit we selected resulting frequencies to

obtain the ‘reconstruction’ signals.

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Figure S1: Results for the Fast-Fourier transform (FFT) spectral analyses for the C-LIP (orange, left) and O-LIP (blue, right) records. The Monte Carlo 95% (or 90%) confidence intervals for each dataset are shown in grey shades. The black number are the Age peaks and grey fields represent the range for significant peaks.

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Figure S2: The 421, 226 and 175 m.y. cycles for O-LIP (blue lines) and The 559, 328 and 163 m.y. cycles for C-LIP (orange lines) are extracted from the FFT using the 500-400, 250-200, 185-165 m.y. bandpasses for O-LIP and the 600-500, 350-300, 170-150 m.y. bandpasses for C-LIP. Also shown is the lifespan of the supercontinent Pangea and Rodinia (Evans et al. 2016).

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1665-870 Ma

MTM methodO-LIPC-LIPs

Figure S3: Results for the multi-taper method (MTM) spectral analyses for the C-LIP (orange, left) and O-LIP (blue, right) records. Also shown are the red noise (red line) and 99%, 95% and 90% of confidence intervals for each dataset. The black number are the Age peaks and grey fields represent the range for significant peaks

0 0.005 0.010 0.015

Frequency (cycles Myr-1)

99%

90%95%

99%

90%95%

SUPPLEMENTARY FIGURES

540-490 Ma 395-360 Ma170-150 Ma 480-520 Ma

420-380 Ma230-190 Ma

1200 Myr495

370165

1000 Myr

400500

210

Figure S4: The 500, 379 and 200 m.y. cycles for O-LIP (blue lines) and the 495, 370 and 165 m.y. cycles for C-LIP (orange lines) are extracted from the MTM. Also shown is the lifespan of the supercontinent Pangea and Rodinia (Evans et al. 2016).. Also shown is the lifespan of the supercontinent Pangea and Rodinia (Evans et al. 2016).

MTMBand-

passes

MTM method

Rel

ativ

e sc

ale

Age (Ma)

PHANEROZOIC

SUPERCONTINENTS

Pangea Rodinia

PROTEROZOIC

NeoproterozoicMeso

proterozoic

0 100 300 500 700 900 1100

95

95

95

525

425

450

475

620

660

775

775

960 1150

1150

1100

275

850

SUPPLEMENTARY FIGURES

500 Ma

379 Ma

200 Ma

500 Ma

400 Ma

210 Ma

495 Ma

370 Ma

165 Ma

495 Ma

370 Ma

165 Ma

Related MTM

peaks

175

120

95 275 450 625 800 975

Table DR1: summary of the main criteria for defining oceanic plume-related basalts in ophiolites

Ophiolite Thicknesshigh-MgO La/Nd TiO2/Yb Nb/Yb Th/Yb REE Pillow lavas Subaerial

meters basalts ppm ppm ppm ppm to PM

Oceanic plateau Lower plate >5000 yes ≤1 >0.6 1 - 10 0.05 - 5 flat may be common occassionaly

Ocean island basal Lower plate <5000 rare ≤1 >0.6 >10 0.9 - 2 LREE ++ few frequently

REE, rare earth elements

Table DR2 of Supplementary Material: Oceanic Large Igneous Provinces Database

2020046_Table DR2.xls

Table DR3 of Supplementary Material: Continental Large Igneous Province record

2020046_Table DR3.xls