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Wjreenhouse and the ORLD MESOZOIC OCEAN SPECIAL ISSUE FEATURE WjREENHOUSE AND THE ORLD MESOZOIC OCEAN BY REISHI TAKASHIMA, HIROSHI NISHI, BRIAN T. HUBER, AMD R. MARK LECKIE Earth's climate has alternated between hurricanes, and enhanced amounts of icant achievements of DSDP and OOP greenhouse (warm) and icehouse (cool) precipitation. Understanding the ocean- research and discusses future prospects modes throughout the Phanerozoic (Fig- climate system during past greenhouse for Integrated Ocean Drilling Program ure 1A). At present, Earth is in the midst climate modes is essential for more accu- (10DP) investigations in the field of Me- of an icehouse climate. Nevertheless, the rately predicting future climate and envi- sozoic paleoceanography. rise of industrialization in the last two ronmental changes in a warming Earth. centuries has led to a dramatic increase The Mesozoic-early Cenozoic is NEW INSIGHTS in atmospheric CO^ from the burning known as a typical greenhouse pe- Determination of Mesozoic Ocean of fossil fuels, which, in turn, has led to riod caused largely by increased CO, Temperature History significant global warming (e.g., Rud- from elevated global igneous activity An important DSDP and ODP achieve- diman, 2000). Global warming could (Figure 1A-C). The mid-Cretaceous is ment was the reconstruction of the his- profoundly impact human life as a result marked by a major warming peak (Fig- tory of Mesozoic ocean temperature of consequent global sea-level rise, more ure 1D); it is characterized by globally changes based on geochemical methods numerous and increasingly powerful averaged surface temperatures more such as oxygen isotopes, TEX^, and al- than 14°C higher than those of today kenone analyses. Oxygen-isotope data Reishi Takashima ([email protected]. (Tarduno et al., 1998), a lack of perma- have provided the greatest source of hokudai.ac.jp) is Research Fellow, Depart- nent ice sheets (Frakes et al., 1992), and paleotemperature reconstructions from ment of Earth and Planetary Sciences, Hok- ~ 100-200-m-higher sea level than that ancient oceans. However, the increasing kaido University, Sapporo,)apan. Hiroshi of today (Haq et al., 1987; Miller et al., prevalence of diagenctic alteration in Nishi is Associate Professor, Department 2005a) (Figure IE). Studies using Deep older or more deeply buried rocks limits of Earth and Planetary Sciences, Hokkaido Sea Drilling Project (DSDP) and Ocean or prevents reliable isotopic data from University, Sapporo, Japan. Brian T. Huber Drilling Program (ODP) cores have being gleaned from biogenic calcite pre- is Curator, Smithsonian Institution, National advanced understanding of Mesozoic served in terrestrial outcrops. Compared Museum of Natural History, Washington, oceanography and climate, demonstrat- to many land-based sections, calcareous D.C, USA. R. Mark Leckie is Professor, ing that Mesozoic ocean circulation and microfossils of Cretaceous age recovered Department of Ceosciences, University of marine ecosystems differed greatly from from samples drilled at DSDP and ODP Massachusetts, Amberst, MA, USA. those of today. This paper reviews signif- sites are often better preserved, and usu- 82 Oceanography I Vol. 19, No. 4, Dec. 2006 Figure 1. Compilation (G) Percent of world's showing the changes original petroleum in climate, and geologi- reserves generated by cal and paleonrologi- source rocks (Klemme cal events through the andlllminshek,1991) Phanerozoic. (F) Percentage extinction (%) of marine genera (Raup and Sepkoski, 1986) and major Oceanic Anoxic Events 20 (E) Sea level changes and continental glaciation (Ridgwell, 2005) (D) Temperature (Frakesetal.,1992) (C) Carbon dioxide Ratio of the mass of atmospheric COj at a past time to that at present (Berner, in press) (B) Production rate of oceanic crust (Stanley,1999) (A) Climate mode (Frakes et al, 1992) i i i i I M i i | i r i i | i i i I I I | I I'I I 0{Ma) 100 200 300 400 500 600 Oceanography I Vol. 19, No. 4, Dec. 2006 83 ally have not been as seriously affected 2003; fenkynsetal., 2004). where the difference of temperature be- by complex tectonic and/or weather- According to isotopic records of sur- tween the mid-Cretaceous and the pres- ing processes. Exquisitely preserved face-dwelling planktic foraminifera, sea ent oceans is nearly 30°C (Figure 2). Bice foraminifera from the low-latitude surface temperatures reached a maxi- and Norris (2002) estimate that at least Demerara Rise (ODP Sites 1258-1261; mum of 42°C at the Demerara Rise (Bice 4500 ppm CO, would be required to 4-15°N), mid-latitude Blake Nose (ODP et al., 2006), 33%: at the Blake Nose (Hu- match the above-mentioned maximum Sites 1049,1050,1052; 30°N), and ber et al., 2002), and 31°C at the Falkland temperatures, which is 11 times greater high-latitude Falkland Plateau (DSDP Plateau (Huber et al., 2002; Bice et al., than the modern atmospheric concen- Site 511; 60°S) in the Atlantic Ocean 2003) during the Turanian (~ 93-89 Ma tration. Using a more recent climate have been especially useful for recon- [million years ago]) (Figures 2 and 3). model, Bice et al. (2006) conclude that structing vertical and latitudinal tem- At comparable latitudes in the modern 3500 ppm or greater atmospheric C02 perature gradients of the mid- through ocean, August surface water tempera- concentration is required to reproduce Late Cretaceous ocean (Figures 2 and 3). tures are 25-28°C at 0-20°N, 20-28°C at the estimated maximum sea surface tem- The TEXS() method is especially useful 20^0°N, and 0-5°C at 60°S (Thurman peratures of the Mesozoic tropical ocean. for organic carbon-rich sediments and and Trujillo, 1999). Consequently, these Because the Mesozoic paleo-tem- has provided excellent paleo-tempera- data suggest that Cretaceous warming perature estimates based on geochemical ture determinations (e.g., Schouten et al., was most prominent at high latitudes proxies are still insufficient in sediments older than Albian (> 112 Ma) and in ar- eas outside of the Atlantic Ocean, further investigations are needed to reconstruct a reliable spatial and temporal tempera- Mid-Cretaceous ture history during the greenhouse cli- 35- sea-su face mate of the Mesozoic. ^ temperature - ? gradient 30 -0' o o Oceanic Anoxic Events Defining the concept of Oceanic Anoxic 25- 8 Events (OAEs) was one of the most im- portant achievements of the early DSDP. 20 o V o m 2L Cretaceous marine sediments in Europe E * V cr are mainly comprised of white lime- i „ 15- * / Present stone and chalk; however, distinct black, " / sea-surface ' temperature laminated organic-rich layers, termed 10 <% ' gradient ,260 390/1049 1257 392 \ "black shales," are occasionally interca- 144 1050 \ fi-533 MS 2 58 511 / 52S356 463,7 '25E 6271052 lated within these sequences (Figure 4). W /' YY W YY \. Y 5 - Because organic carbon is preferentially 1— —I— —I I 1 1 T 1 1 80*S GO'S 40"S 20°S 0 20°N 40° N 60"N 80"N preserved under anoxic conditions, ear- Latitude lier workers suggested that these black y ODP/DSDP sites Y other core sites shales had accumulated locally in a Paleo sea surface temperature weakly ventilated, restricted basin under ^Maastrichtian OTuronian DCenomanian Alate Albian regional anoxic conditions. In the mid- 1970s, however, the discovery of black Figure 2. Latitudinal variations of surface ocean paleo temperature derived from oxy- gen isotopes of planktonic foraminifera and TEX^. Modified from Huber etal. (2002), shales at many DSDP drill sites from Bice et a I. (2003), and Jenkyns et al. (2004). the Atlantic, Indian, and Pacific Oceans 84 Oceanography I Vol.19, No. 4, Dec, 2006 led to recognition of widespread anoxic Burial of organic carbon, which pref- trial rocks such as dark gray- to black- conditions in the global ocean spanning erentially sequesters iso topically light colored mudstones, carbon isotope limited stratigraphlc horizons (Figure 5). carbon during OAEs, resulted in a posi- excursions are a useful marker for rec- Schlanger and Jenkyns (1976) termed tive 513C (13C/12C) excursion of 2-3%o ognizing OAEs (e.g., Groke et ah, 1999; these widespread deposit tonal black in the geologic record (Figure 3). Even Takashima et ah, 2004). Recent advances shale intervals "Oceanic Anoxic Events." if black shales are not visible in terres- in biostratigraphy and correlation us- Bulk Carbon Isotope Ocean Crust Production Paleo-temperature (Huberetal.,2002) [green line} Sea Level and Carbonate Platform (Stanley and Hardie 1998) Blake Plateau S. high latitude Oceanic Anoxic Cm) 2 Drowning [rEd arrow) (km /year) [Site 1049) (Site 511 and 690) Events 0 Oarnonarp 10 14 IB 22 26 30 <*C) 6 10 14 18 22 26 CO J I I I I I J I I I I I l_ • • - % V> A% Caribbean Plateau 1 00°0 tfi O O Of Kerguelen Plateau I P,aj ma rial Trap ~* Ontong • Benthk foraminifera Q Plankricforaminifera Parana H Flood Karoo Flood Basalt Circum Atlantic L Magmatic Province I I I 4 6 (x10skms) Large Igneous Provinces {Jones and Jenkyns, 2001) Figure 3. Compilation showing Jurassic-Cretaceous changes in sea level, oceanic-crusc production, pa I eo-temperature, bulk carbon isotopes, carbonate- platform drowning events and OAEs. Large Igneous Province data are from Jones and Jenkyns (2001), Bulk carbon isotopes are from (1) Van de Schoot- brugge et al. (2005); (2) Hesselbo et ai. (2000); (3) Morettini etal. (2002); (4) Dromart et al. (2003); (S) Weissercet at (1998); (6) Erbacher et al, (1996); (7) Jenkyns et al. (1994); (8) Jarviset ai, (2002); and (9) Abramovich et al. (2003). Carbonate-platform drowning data are from Simo et al. (1993) and Weis- sert and Mohr (1996), Oceanography I Vol. 19, No. 4, Dec, 2006 85 Figure 4. Cretaceous black shales intercalated in pelagic limestone sequence, central Italy. Figure courtesy of R. Cocci on i.
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