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Supplementary tableName Ref. Proxy Conversion Duration 4t lon lat1. Clim. Anl. Cent. [1] instrum. N/A 33 1/12 global —2. Clim. Res. Unit [2] instrum. N/A 135 1/12 global —3. Rarotonga Coral [3] Sr/Ca −4◦/(mmol/mol) 270 1/12 -160 -214. W167-79 Sed. [4] δ18O 4◦/mil 5210 21 -83 245. ODP658 Sed. [5] foram asmb. — 14700 109 -18 206. PL07-39 Sed. [6] Mg/Ca — 24500 134 -65 117. OCE205-103 Sed. [7] δ18O 4◦/mil 51600 273 -79 278. EW9209-1 Sed. [8] δ18O 4◦/mil 190000 632 -43 59. TR163-19 Sed. [9] Mg/Ca — 360000 1740 -90 210. ODP6777 Sed. [10] δ18O 4◦/mil 771000 1840 -43 611. ODP846 Sed. [11] alkenones — 1830000 2000 -90 312. ODP927 Sed. [12] δ18O 4◦/mil 772000 2200 -43 613. ODP806 Sed. [9] Mg/Ca — 46600 2440 159 214. NCEP [13] instrum. N/A 55 1/12 — —15. Clim. Res. Unit [14] instrum. N/A 135 1/12 — —16. Cent. England [15] instrum. N/A 345 1/12 0 6017. Donard Lake [16] varve thick. — 1240 1 -61 6718. Taylor Ice [17] δ18O 1.5◦C/mil 209000 65 158 -7719. GISP2 Ice [18] δ18O 1.85◦C/mil 111000 79 -39 7320. Byrd Ice [19] δ18O 1.5◦C/mil 79800 109 -120 -8021. Vostok Ice [20] δD — 423000 128 107 -7822. Dome C Ice [21] δD 0.2◦C/mil 740000 910 124 -75Table S1: Instrumental, tropical sea surface temperature proxies, and high-latitude surface air temper-ature proxies used to estimate temperature variability. Each group is ordered according to samplingresolution. From left to right are the record designation, a primary reference, observation method, theconversion used for temperature, duration in years, mean sampling interval in years, longitude in◦E,and latitude in◦N. Temperature conversions listed as “—” are nonlinear and are provided by the citedreference. Conversion for GISP2 is from [22] and for Taylor and Byrd from [23]. The marine δ18Ocalciteconversion is from [24]. Rarotonga temperature conversion is determined by adjusting the level of thebackground spectra to that of average tropical pacific instrumental records from [1]. Fig S2 shows thespectral estimate associated with individual records.Supplementary figures and legendsThe NCEP reanalysis of surface air temperatures has the advantage of being global, but relies upona spectral model, introducing concerns regarding the accuracy of the surface temperature spectra. Thus,a complimentary analysis is c onducted (see Fig S1) using the CRU compilation of instrumental surfaceair temperature records [14]. The CRU compilation is not globally resolved, but has the advantage ofcontaining records extending back as far as 1870. NCEP, proxy, and CRU results all agree with oneanother. Fig S2 shows the spectral estimates for individual proxy and instrumental records used ingenerating Fig 2.1longitudelatitude 180oW 120oW 60oW 0o 60oE 120oE 180oW 60oS 30oS 0o 30oN 60oN (b)10.80.60.40.2latitude 180oW 120oW 60oW 0o 60oE 120oE 180oW 60oS 30oS 0o 30oN 60oN (a)22.533.544.555.566.510−210−1100101102103frequency (1/years)energy (o C2/ds)(c)Figure S1: Temperature scaling at instrumental periods from the CRU compilation of instrumentalsurface air temperature records. (a) Map of the energy at the annual cycle in log-base-ten◦C2/ds. (b)β computed between 1 month and 100 years after removing the energy associated with the annual cycleand its higher harmonics. Note that the scaling indicated by the colorbar is inverted. (c) Spectra binnedaccording to annual period energy and averaged. In this case, the annual cycle and its higher harmonicsare removed prior to averaging, unlike in fig 1. Black lines indicate power-law fits to the continuum.The axes are logarithmic and the shading corresponds to the colorbar in panel a. The β and averagemagnitude of the continuum both scale with the annual variability and are in agreement with the NCEPresults.210−410−2103104105106107108δ18OiceTaylor Ice Core10−410−2103104105106107δ18OiceByrd Ice Core10−410−2103104105106107108δ18OiceGISP2 Ice Core10−410−2103104105106107108δDVostok Ice Core10−410−2104105106107108δDDome C Ice Core10−2100102103104varve thicknessDonard Lake10−2100102103104105106107108109instrumentalCentral England Thermometer10−410−2105106Mg/CaTR163−19 Sed. Core10−410−2105106Mg/CaODP806 Sed. Core10−410−2103104105Mg/CaPL07−39PC Sed. Core10−410−2103104δ18OcalFlorida Straits Sed. Core10−410−2105106107δ18OcalODP927 Sed. Core10−410−2105106107δ18OcalODP6777 Sed. Core10−410−2103104105106δ18OcalOCE205−103GGC Sed. Core10−410−2105106107δ18OcalEW9209−1JPC Sed. Core10−410−2104105106107alkenonesODP846 Sed. Core10−410−2103104105foram assemblageODP658 Sed. Core10−410−2103104105foram assemblageODP658 Sed. Core10−2100101102103104105106107Sr/CaRarotonga CoralFigure S2: Spectral energy estimates for individual proxy and instrumental temperature records. Thefirst seven panels are for high-latitude land temperatures and the last twelve are for tropical sea-surfacetemperatures. The title gives the name of each record and the y-axis indicates the data type. The y-axisis in units of◦C2/ds and the x-axis is in units of cycles/year. Axes are logarithmic. Daggers in the upperright hand portion of e ach plot indicate the approximate 95% confidence level, where the horizontaldash indicates the level of the background continuum. Fig 2 shows these spectra plotted together afteraveraging according to data type. Data types are grouped by color.3References[1] Reynolds, R. A real-time global sea surface temperature analysis. Journal of Climate 1, 75–86(1988).[2] Parker, D., Folland, C. & Jackson, M. Marine surface temprature: observed variations and datarequirements. Climatic Change 31, 559–600 (1995).[3] Linsley, B., Wellington, G. M. & Schrag, D. Decadal sea surface temperature variability in thesub-tropical South Pacific from 1726 to 1997 a.d. Science 290, 1145–1148 (2000).[4] Lund, D. & Curry, W. Late Holocean variability in the Florida Current surface density: Patternsand possible causes. Paleoceanography 19, 10.1029/2004PA001008 (2004).[5] de Menocal, P., Ortiz, J., Guilderson, T. & Sarnthein, M. Coherent high- and low-latitude climatevariability during the Holocene Warm Period. Science 288, 2198–2202 (2000).[6] Lea, D., Pak, D., Peterson, L. & Hughen, K. Synchroneity of tropical and high-latitude Atlantictemperatures over the last glacial termination. Science 301, 1361–1364 (2003).[7] Curry, W. & Oppo, D. (unpublished data).[8]


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