Ilya Bindeman, University of Oregon
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1 Snowball or Slushball Earth Glaciation 2.4Ga? Resolving microanalytical evidence in subglacially hydrothermallyaltered (down to δ 18 O) rocks and coeval supergene materials Ilya Bindeman, University of Oregon Collaborators: A.K. Schmitt (UCLA), D.A.D. Evans (Yale), N.S. Serebryakov (Moscow), A. Bekker (Manitoba) Thanks to: P. Hoffman ( U Victoria), Guan B, J Eiler (Caltech) J Vazquez (USGS) NSF grant EAR Snowballearth.org 1
2 Valley et al.,
3 The world record : 2.45Ga, δ 18 O metagabbro/gneisses from Karelia, Russia δd= -235 Global Distribution of water isotopes Karelian values 3
4 Comparison with Modern climates -25 and below... Greenland-like, -20 C to -35 C 5 Rock
5 A! Belomorian Belt In 2.4 Ga gabbro 2.6 Ga gneiss The lowest isotope values: 5
6 Grt-Bi Ky-Grt-Bi Ruby-Grt-Bi Grt-gabbro
7 Old isotope sampling map 2011 and 2012: Red low δ 18 O Yellow- normal 7
8 Isotope Profiles in other localities: Bindeman and Serebryakov, EPSL, 2011 Equilibrium within crystal clusters, δ 18 O heterogeneity on cm, m, 10 m scales 8
9 Bull s Eye patterns are very common in ore deposits (Taylor, 1973, 1974), in Skaergaard Intrusion (Taylor and Forester 1979) Explanation: Rifting under ice 9
10 Summary of field/geological observations 2.6 Ga Gneiss, 2.4 Ga mafic intrusions, 1.9 Ga metamorphism Depletions of δ 18 O and δd are in or near contacts with Ga mafic intrusions These intrusions are related to rifting Depletions of δ 18 O and δd form bull s eye concentric pattern, characteristic of modern hydrothermal systems Depleted localities occur over 220 km Tectonic Story Zircon Story! 2.6Ga Normal-δ 18 O matrix, zircon 2.4 Ga hydrothermal alteration Low-δ 18 O matrix ca -27 Intact 2.6 Ga, +7 zircon 1.9Ga metamorphism Low-δ 18 O matrix, 1.9Ga, -27 rims Bindeman et al in press 10
11 Methods Karelian samples firmly belong to the Equilubrium terrestrial 18 O/ 16 O - 17 O/ 16 O fractionation line 10 00*ln(1+d17O/10 00) Karelia 1 7-O va ria tion s 10 y = x R 2 = TFL *ln(1+d18O/1000) 11
12 Cometary Impact? No: Δ 17 O = 0 Analysis of individual minerals in crystal clusters Bindeman et al
13 Isotope Mapping of a single corundum crystal Hydrogen Isotopes Insights - record low δd of -235 Fig. 5 13
14 2.4Ga Subglacial Rifting Karelia in the Paleoproterozoic: Bindeman Schmit Evans
15 Paleoprot. glacial deposits a"er assembly in the Nuna supercon4nent Figure from Young,
16 Using zircon to resolve the timing of δ 18 O depletion Perfect mineral to retain U-Pb age and δ 18 O values Requires high T (ca>650 C) to recrystallize or exchange O So it only records magmatic or metamorphic episodes Untouched by hydrothermal alteration Dating synglacial intrusions = Dating glaciations (and rise of atmospheric oxygen) 16
17 Zircon Story: 2.6Ga rock 2.4 Ga hydrothermal alteration Normal-δ 18 O matrix, zircon 1.9Ga metamorphism Low-δ 18 O matrix ca -27 Intact 2.6 Ga, +7 zircon Low-δ 18 O matrix 2.6 Ga, +8 zircon cores, 1.9Ga, -27 rims When did the δ 18 O depletion happen? Supercontinents: Nuna Superia Glacials rims K5 Rifting, hydrothermal alteration Rifting, hydrothermal alteration rims AB
18 18
19 How did it happen? Do Karelian rocks record Snowball or Slushball Earth? 19
20 δ 18 O water, Tiny amounts, Mixed with snowflakes -11? Jormangund Climate State (2011): Dorian Abbot (U Chicago) 20
21 Modern Jormangund Hard- Snowball 21
22 Slush-Ball vs Hard Snow Ball Earth climate models and implications 22
23 18 O/ 16 O in Global Circulation Model of Slushball Earth δ 18 O, Jun-Eun Lee and Bindeman in prep. 23
24 T a nd d18o vs latitude Latitude, degrees Karelian Position Over continent Equator T' C d1 8O, pr ecipi tati on Over Ocean T or d18o, SMOW Conclusions and what s next? - Kareilan Gneiss record depletion during ~2.4 Slushball Earth or Jurmangand episode (the first of the 3) to allow for effective vapor δ 18 O, δd distillation - What is next? We are trying to find sedimentary rock that would correspond in age to the Slushball Earth episode - Testing stability of the Slushball Earth model is required 24
25 Supracrustal Materials that may record δ 18 O water : - Secondary Quartz Amygdaloids - Glacial Rock flower - Pillow basalts - Shales Comparison with Antarctica 25
26 Why most depleted oxygen isotopes are found in midto ultrahigh-pressure metamorphic rocks? - Dabie Shan -Sulu (China) coesite-bearing eclogites, -10 to +2 (Rumble and Yui, 1998; Zheng et al ) Ma 500 papers published on δ 18 O in Dabie Shan! - Kokchetav (Kazakhstan), coesite-bearing, down to -3.9 (Masago, Rumble et al 2003) Ma Now Karelia -27! Mid grade kyanite-bearing gneisses Ga Bindeman et al., 2013 in press 26
27 Oxygen isotopic values of diamond-bearing, exhumed UHP metamorphic rocks: Mostly high-δ 18 O Fiordfelt +7.3, Erzgebirge Alpe Arami Makbal +6.9 Kumdikul +6.6 Rodopi Sederonero Sample collection of Larissa Dobrzhinetskaya, UC Riverside How long does it take? 27
28 Modeling Chemical change to make high-al lithology Dissolution in 200 C fresh water Reed et al. Chiller Program Fig. A Retrogression of oxygen isotopic values in a typical corundum bearing assemblage as a function of cooling and d ifferential closure using Fast Grain Boundary diffusion model of Eiler, Baumgartner, and Valley, (1993). Notice that even at slow cooling rate of 1 degree per million years corundum, garnet, hornblende, staurolite, and kyanite do not retrogress and preserve their original, peak metamorphic temperature of formation. Plagioclase, rutile, and biotite display retrogression of less than 0.7 permil. Sizes of minerals and their proportions are given in the table. At faster cooling rate even less retrogression is expected. Therefore, Isotope heterogeneity observed within hand specimen (see Table A1 and Bindeman et al. 2010, Fig. 2) cannot be explained by differential retrogression and must reflect source variability and interaction with external fluids. 28
29 Extra Generic Snowballearth slides from Snowballearth.org Paleoproterozoic? 29
30 Paleoproterozoic Glaciations Hydrologic Cycle on Snowball Earth? None 30
31 Vaalbara supercraton Paleomag. (De Kock et al., 2009) Meteorite Bore Member, Kungarra Fm (Pilbara) Makganyene Fm (Kaapvaal) Paleoproterozoic glacial deposits original distribu4on in the Superia supercraton reassembled in Nuna Ch Hn C Figure a2er Ernst & Bleeker 2008 S Hw K 31
32 Stratigraphic column of the Huronian Supergroup in Ontario, Canada (modified from Bekker et al., 2006: One OR Three Glaciations? 2.32Ga 2.4 Ga Karelia Glaciation Glacial paleolatitudes darker shade indicates more reliable paleomagnetic data Paleoproterozoic units Meteorite Bore: 05 Makganyene: 11 Gowganda: 03 (?) Sariolian:
33 a b c d e Field relations between different rock types: a) original Chupa gneiss; b) St-Pl pseudomorphs over large crystal of Ky at Khitostrov; c) rock with large Crn; d) St-Pl pseudomorphs over large crystal of Ky at Khitostrov; d) Corundum-bearing rock (pen is pointing to Crn), impregnated by plagioclazite at Khitostrov; e) large crystals of garnet in chloritic rock inside amphibolite at Mt. Dyadina. 33
Department of Geological Sciences, 1272 University of Oregon, Eugene, Oregon 97403, USA 2
Field and microanalytical isotopic investigation of ultradepleted in 18 O Paleoproterozoic Slushball Earth rocks from Karelia, Russia I.N. Bindeman 1, N.S. Serebryakov 2, A.K. Schmitt 3, J.A. Vazquez 4,
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