OCEAN DRILLING PROGRAM LEG 184 SCIENTIFIC PROSPECTUS SOUTH CHINA SEA Dr. Warren L. Prell Co-Chief Scientist Department of Geological Sciences Brown University Box 1846 Providence, RI 02912 U.S.A. Dr. Pinxian Wang Co-Chief Scientist Department of Marine Geology Tongji University Shanghai 200092 People's Republic of China Dr. Peter Blum Staff Scientist Ocean Drilling Program Texas A&M University Research Park 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Jack Baldauf Deputy Director of Science Operations ODP/TAMU Peter Blum Leg Project Manager Science Services ODP/TAMU September 1998 Material in this publication may be copied without restraint for library, abstract service, educational, or personal research purposes; however, republication of any portion requires the written consent of the Director, Ocean Drilling Program, Texas A&M University Research Park, 1000 Discovery Drive, College Station, TX 77845-9547, U.S.A., as well as appropriate acknowledgment of this source. Scientific Prospectus No. 84 First Printing 1998 Distribution Electronic copies of this publication may be obtained from the ODP Publications homepage on the World Wide Web at: http://www-odp.tamu.edu/publications D I S C L A I M E R This publication was prepared by the Ocean Drilling Program, Texas A&M University, as an account of work performed under the international Ocean Drilling Program, which is managed by Joint Oceanographic Institutions, Inc., under contract with the National Science Foundation. Funding for the program is provided by the following agencies: Australia/Canada/Chinese Taipei/Korea Consortium for Ocean Drilling Deutsche Forschungsgemeinschaft (Federal Republic of Germany) Institut Francais de Recherche pour l'Exploitation de la Mer (France) Ocean Research Institute of the University of Tokyo (Japan) National Science Foundation (United States) Natural Environment Research Council (United Kingdom) European Science Foundation Consortium for the Ocean Drilling Program (Belgium, Denmark, Finland, Iceland, Italy, The Netherlands, Norway, Portugal, Spain, Sweden, and Switzerland) People's Republic of China Any opinions, findings, and conclusions or recommendations expressed in this publication are those of the author(s) and do not necessarily reflect the views of the National Science Foundation, the participating agencies, Joint Oceanographic Institutions, Inc., Texas A&M University, or Texas A&M Research Foundation. This Scientific Prospectus is based on precruise JOIDES panel discussions and scientific input from the designated Co-chief Scientists on behalf of the drilling proponents. The operational plans within reflect JOIDES Planning Committee and thematic panel priorities. During the course of the cruise, actual site operations may indicate to the Co-chief Scientists and the Operations Manager that it would be scientifically or operationally advantageous to amend the plan detailed in this prospectus. It should be understood that any proposed changes to the plan presented here are contingent upon approval of the Director of the Ocean Drilling Program in consultation with the Science and Operations Committees (successors to the Planning Committee) and the Pollution Prevention and Safety Panel (PPSP). Technical Editor: Karen K. Graber ABSTRACT During Leg 184 we will core hemipelagic sediments in the South China Sea (SCS) to determine the evolution and variability of the East Asian monsoon during the late Cenozoic. Of the six primary proposed drill sites, five are located on the northern continental slope of the SCS in water depths ranging from 1265 m to 3190 m. In the southern SCS, one site will be located on the southern margin in 2830 m water depth. The major goals of Leg 184 are to improve our knowledge about the variability of monsoonal climates, including millennial to possibly centennial variability from high-sedimentation rate records (SCS-1), orbital-scale variability from records at all SCS sites, and tectonic-scale variability from late Cenozoic sections (Sites SCS-4 and 5). The records from the SCS will be used to establish the links between the East Asian and Indian monsoons and to evaluate mechanisms of internal (climate system feedbacks) and external (orbital and tectonic) climate forcing. We seek to test a suite of hypotheses that link uplift of the Himalayan and Tibetan Plateau complex (HTC) to both the intensification of the Asian monsoon and late Cenozoic global cooling. The proposed drilling program in the SCS will enable comparison of the Chinese terrestrial record with the marine records of monsoonal climates and hence provide an additional regional constraint on the scenarios for monsoon evolution. Leg 184 has a number of related major scientific objectives: 1.obtain continuous sequences of hemipelagic sediments that record the East Asian climate history during the late Cenozoic; 2. establish records of monsoonal proxies for the SCS, including the variability of sediment properties, the rates of sediment accumulation, and the chemical, isotopic, and species variability of flora and fauna; 3.establish stratigraphic ties between the SCS marine record and the terrestrial records of China; 4.establish the relationship of East Asian monsoon variability with orbital forcing, glacial forcing, and internal feedbacks within the climate system; 5.compare the evolution of the East Asian monsoon in the SCS with the Indian monsoon in the Arabian Sea to identify common causality; 6.test several proposed scenarios for the relationship between the Tibetan Plateau uplift, monsoon evolution, and global cooling; and 7. improve our understanding of seasonality in the low-latitude SCS and how it relates to the stability of the Western Pacific Warm Pool and the strength and evolution of the winter monsoon. INTRODUCTION The Asian monsoon is one of the major components of the global climate system and its evolution plays a significant role in our understanding of global climates (Fig. 1) (Hastenrath, 1991; Hastenrath and Greischar, 1993; Webster, 1987; Webster, 1994; Webster et al., 1998). The Asian summer and winter monsoons dominate the seasonal winds, precipitation and runoff patterns, and the character of land vegetation over southern and eastern Asia. The winter monsoon is characterized by high pressure over northern Asia, northeast winds across the South China Sea (SCS) (which intensify during cold surges), and enhanced precipitation in the Austral-Asian equatorial zone (Fig. 1A, 1C). The summer monsoon circulation is characterized by low pressure over Tibet, strong southwesterly winds, upwelling in the Arabian Sea, and high precipitation over southern and eastern Asia (Fig. 1B, 1D). The SCS is ideally located to record the paleoceanographic responses to both winter and summer monsoons (Figs. 1, 2). Evolution of the Asian monsoon system is thought to reflect at least four types of large-scale climate forcing or boundary conditions: (1) the tectonic development of the Himalayan-Tibetan orography, (2) changes in the atmospheric CO2 concentration, (3) changes in the Earth's orbital parameters and the resulting variations in seasonal solar radiation, and (4) changes in the extent of glacial climates. These factors act to amplify or dampen the seasonal development of land-sea heating and pressure gradients, latent heat transport, and moisture convergence over the Asian continent. Mountain-Plateau Uplift Forcing The effects of tectonically induced orographic changes on the monsoon system provide an explanation for its initiation, intensification, and long-term (106 yr) evolution (see the papers and references in Ruddiman, 1997). Prior to the collision of India with Asia, the Himalayas and Tibet did not exist in their present state, and the Asian continent was not as large. The smaller size and lower elevations of the pre-collision continent might be expected to support a lower land-sea heating contrast because of the important role of sensible heating over the plateau and the condensational heating over and on the flanks of the Tibetan Plateau. In general, the modern monsoon circulation would not exist if the Himalayas and Tibet were not at their present location and elevation. For the summer monsoon, the thermal effects, both sensible and latent heating, of the Himalayan and Tibetan Plateau complex (HTC) are the major impact of the orographic forcing. During the winter monsoon, the thermal effects of the HTC are thought to be small, but the mechanical effects, such as blocking and directing low-level winds and the development of cold surges, are the major impacts of the orography (Murakami, 1987). The SCS should provide an especially good record of the winter monsoon evolution and its relationship to the evolving orography of Asia. CO2 Forcing A variety of observations have suggested that CO2 levels were higher during the Tertiary and may have been equivalent to double the present CO2 levels at ~20 Ma (see Kump and Arthur, 1997 and other papers in Ruddiman, 1997). Higher CO2 levels might be expected to strengthen the summer monsoon through increased land-sea contrasts and more active hydrologic budgets but might also weaken the winter monsoon through warmer continents. Lowered CO2 levels are thought to have caused global changes in vegetation from C3 to C4 ~7 Ma (see Fig. 3), which also has implications for monsoonal processes related to soil moisture, albedo, and carbon cycling (Cerling, 1997). Hence, the strength of winter monsoons in the SCS may covary with both increased orography and decreased CO2. Orbital Forcing Changes in the Earth's orbit result in redistribution of solar energy over the surface of the Earth. For example, during high eccentricity intervals the precessional-driven summer season radiation budget over the Tibetan Plateau can vary as much as +12.5% (relative to modern values of 450 W/m2). Numerous studies of Indian Ocean and western Pacific sediments reveal that a number of monsoon indicators (upwelling fauna, productivity, dust particle size, and vegetation types) vary coherently with orbital periodicities (Prell, 1984a, 1984b; Clemens et al., 1991; Morley and Heusser, 1997). However, the monsoonal indices are not always in direct proportion or in phase with the apparent solar forcing. The phase of monsoonal responses in the SCS should provide additional constraints on the relative importance of orbital forcing and internal feedbacks on monsoonal variability. Glacial Climate Forcing The extent of glacial-age surface boundary conditions also affects the monsoon system (Prell and Kutzbach, 1987, 1992). Numerous studies have shown that more extensive glacial climates tend to weaken the summer monsoon (Clemens et al., 1996), although glacial intervals do contain strong monsoons (Clemens and Prell, 1991). These responses result from the lower sea surface temperature, lower sea level, higher albedo of the land surface, and the extent and elevation of large ice masses (CLIMAP, 1976, 1981). However, more extensive glacial climates may strengthen the winter monsoon, especially as recorded in the SCS. Given these potential "causal" factors, our goal is to understand their relative importance in the initiation, evolution, and variability of the Asian monsoon system. Hence, one of the long-term goals of Leg 184 is to decipher how the tectonic development of Asia, the Asian monsoon circulation, and global climate have co-evolved during the Neogene. Despite the importance and interconnections of the two monsoonal subsystems (East Asian and Indian), previous marine-based studies of past monsoonal variations have concentrated on the Indian monsoon (Prell, Niitsuma, et al., 1991; Prell et al., 1992 and references within). The East Asian paleomonsoon studies have been restricted mainly to land-based work, with monsoon information commonly being obtained from the Chinese loess. Less attention has been paid to the marine aspects of the East Asian monsoon until recently. Extensive hydrocarbon exploration in China and its surrounding offshore areas has accumulated extensive geological data that are rich in Cenozoic paleomonsoon information. Together with recent progress in Quaternary science for East Asia and the western Pacific (e.g., Liu and Ding, 1993; Wang, 1990), the data have led to the development of a four-stage model of East Asian monsoon evolution: a premonsoon stage (Paleocene and early Eocene), a transitional stage (late Eocene to Oligocene), a monsoon Stage I (Miocene and Pliocene), and a monsoon Stage II (late Pliocene [2.4 Ma] to present) (Table 1; Wang, 1997). Palynologic, paleobotanic, and lithologic data (Fig. 4C) indicate that the climate pattern in China underwent a profound reorganization around the beginning of the Neogene (Wang, 1990; Sun and Wang, pers. comm., 1998). The Paleocene in China inherited the Late Cretaceous environmental pattern ("Pre-monsoon Stage"), with a broad arid zone traversing the whole country from west to east (Fig. 4A). The middle-late Eocene and Oligocene climate in China ("Transitional Stage") was characterized by variable, weak summer monsoons that brought moisture to the otherwise dry areas, which created the most favorable conditions for nonmarine oil accumulation in China. During the Miocene, the arid zone retreated to northwest China, and eastern China became more humid (Fig. 4B; "Monsoon Stage I") as the southeast summer monsoon strengthened and brought moisture from the sea. This general regime has existed from the Miocene to the Holocene. The intensification of the winter monsoon in eastern Asia is thought to occur much later, and to have marked the beginning of deposition of the Chinese loess deposits at about 2.4 Ma ("Monsoon Stage II"; Liu and Ding, 1982). The loess deposits are a joint product of winter and summer monsoons and thus imply that both systems are active. However, some recent studies suggest that the eolian component of the loess red-clay sequence may have began as early as 7 Ma (Ding et al., 1998), which would have implications for the tectonic vs. glacial initiation and intensification of the winter monsoon. Among the continents of the world, Asia has been subjected to the most significant Cenozoic deformation. The Cretaceous-Paleocene topography of China was generally tilted to the west, with the coastal areas of the Tethys in the west and relatively high land and endorheic basins in the east. This paleogeographic pattern lasted until the late Eocene when India collided with Asia, thereby bringing the maritime conditions in western China to an end. The uplift of the Tibetan Plateau may have started about 21-20 Ma (Copeland et al., 1987; Harrison et al., 1991) and was accompanied by a general subsidence of East China. Other studies (Molnar et al., 1993) suggest that the Tibetan Plateau was uplifted rapidly about 10 Ma and has been subsiding since the middle Miocene. These tectonic changes led to a reversal of the topographic trend in China from west tilting to east tilting, with the west-east gradient in altitude increasing continuously since then. In addition, the early Miocene was also the time of formation for many of the western Pacific marginal seas. The radical changes that occurred in the topography of Asia during the Cenozoic must have had a profound impact on climate, including the onset or strengthening of the monsoon circulation in East Asia. The further development of east-sloping topography and monsoon precipitation has brought about the large river systems, which discharge enormous amounts of sediments into the newly formed marginal seas along the East Asian coast and build extensive coastal plains and continental shelves. Because the Indian and East Asian monsoons share the same tectonic factor in their evolution, we would expect to find synchronous evolutionary stages. Deep Sea Drilling Project (DSDP) and Ocean Drilling Program (ODP) core studies have revealed the onset of clastic deep-sea fan sedimentation at about 20 Ma, which may be related to monsoon runoff (Cochran, 1990). Both marine and terrestrial data indicate a major intensification of the Indian monsoon around 8 Ma (Fig. 3) (Prell, et al., 1992 and references within; Prell and Kutzbach, 1992). If the East Asian monsoon record in the SCS supports this timing, it will be a strong argument in support of tectonic forcing as a cause for intensification of both Asian monsoons. The accelerating uplift of the Tibetan Plateau is thought to be responsible not only for the intensification of the Asian monsoon, but also for late Cenozoic global cooling (e.g., Ruddiman and Kutzbach, 1989). Raymo et al. (1988) proposed that long-term increased chemical erosion in rapidly uplifted areas could reduce atmospheric CO2 (Raymo, 1994) and thereby cool the planet and enable widespread glaciation. If this is the case, the evolution of Asian monsoon and global cooling should be correlated with each other. The proposed drilling in the SCS will test for causal relationships between the three major environmental features in the late Cenozoic (1) global cooling, (2) enhanced chemical and physical weathering, and (3) onset/intensification of the Asian monsoon. GEOLOGIC FRAMEWORK FOR THE SOUTH CHINA SEA Tectonic Setting The opening of the SCS was genetically related to the deformation of Asia. The rhomboid-shaped Central Basin is the major deep-water oceanic crust feature of the SCS (Fig. 5A). Judging from the magnetic anomalies in the SCS Central Basin, seafloor spreading lasted from 32 Ma (magnetic Anomaly 11) to 16 Ma (Anomaly 5c), with a southward ridge jump at ~27 Ma (Anomaly 7/6b) (Briais et al., 1993). The opening of the SCS basin is thought to be linked with the Red River fault zone, which has at least 500 to 600 km of left-lateral displacement during the Oligocene and Miocene (Sch„rer et al., 1990; Briais et al., 1993). The slopes of the SCS contain numerous coral reef terrain systems that migrated during the SCS opening: the Nansha Terrain (Reed Bank and Dangerous Ground), the Xisha-Zhongsha Terrain (Macclesfield Bank and Paracel Island) and others (Jin, 1992). The northern continental margin of the SCS has been extensively studied as part of oil exploration and geophysical studies to determine the amount of crustal extension during formation of the SCS (e.g., Hayes et al., 1995). The sedimentary basins of the northern shelf show a typical double-layer structure, with a lower section characterized by half grabens formed during Paleogene rifting and an upper section characterized by a wider distribution of deposits formed during the broad subsidence in the Neogene (Fig. 5B; Ru et al., 1994). Sedimentology and Stratigraphy Modern sediments in the SCS consist mainly of terrigenous material, biogenic carbonate and opal, and a small portion of volcanic material. Clastic sediment is mainly discharged into the SCS from the Mekong River, Red River, and Pearl River. However, during the past glacial intervals, the paleo-Sunda River system provided a great amount of sediment into the SCS. Recent sediment trap studies in the northern SCS have shown that the highest particle-flux rates are correlated with high wind speed during the winter monsoon and, hence, the suspended matter from the East China Sea and the Pacific may exceed the amount of river input into the northern SCS (Jennerjahn et al., 1992). With the high terrigenous input and the location of the modern carbonate compensation depth (CCD) at 3500 m, the extensive continental slopes of the SCS are dominated by hemipelagic sediments; whereas, the deep-sea basin is covered by abyssal clay, and biogenic carbonates are found around coral reef islands. Two types of carbonate cycles are found in the late Quaternary SCS: the "Atlantic" type (above the lysocline), where the controlling factor is dilution by terrigenous clasts, and the "Pacific" type (below the lysocline), where deep-sea dissolution is the controlling factor (Wang et al., 1986; Bian et al., 1992; Thunell et al., 1992; Zheng et al., 1993; Miao et al., 1994; Wang et al., 1995b). The shelf basins on the SCS contain thousands of meters of Cenozoic deposits that have been drilled by petroleum companies. The basins have nonmarine sequences underlying marine sediments that were deposited during the Miocene or late Oligocene (Fig. 6). Reworked Paleocene and Eocene marine microfossils were present in Neogene deposits from the northern shelf, and Paleocene deltaic and Eocene marine sediments were found in the southern part of the SCS (Fig. 6) such as the Liyue Bank (Reed Bank) Basin, where carbonate deposition started from the middle Oligocene (ASCOPE, 1981; Jin, 1989). Among the basins in the northern SCS, the Pearl River Mouth Basin is the most studied. Over 150 wells have been drilled there and a detailed stratigraphy established for the marine sequence from the uppermost Oligocene to Pleistocene on the basis of various groups of planktonic microfossils (Huang, 1997). Of particular interest are the boreholes drilled on the continental slope in water depths over 500 m, such as Well BY 7-1-1, where the marine sequence ranges from NP23/24 to NN20 (see fig. 3 in Huang, 1997). On the basis of recent publications (Jiang et al., 1994; Wu, 1994; Huang, 1997), the Cenozoic stratigraphy of the Pearl River Mouth Basin is summarized in Figure 6. Noticeable is the presence of nonmarine intercalations in the northern part of the basin, thinning out and decreasing in proportion southward toward the deeper part of the slope. Major depositional hiatuses have been observed at least in the lower part of the lower Miocene, near the end of the middle Miocene, and around the Plio- Pleistocene boundary (L. Huang, pers. comm., 1998). Late Quaternary Paleoceanography During the last glacial maximum (LGM), sea-level lowering caused remarkable alteration in the configuration and area of the western Pacific marginal seas. The three major shelf areas that emerged during the LGM (East China Sea Shelf, Sunda Shelf or the Great Asian Bank [Fig. 7A], and Sahul Shelf or the Great Australian Bank) amount to 3,900,000 km2, which is comparable in size to the Indian subcontinent. The SCS lost half of its area (>52%) as a result of shelf exposure, which changed its configuration into a semi-isolated basin (Wang et al., 1997). Moreover, the most extensive shelf area of the SCS is located in the modern Western Pacific Warm Pool bounded by the 28¡C surface isotherm. The reduction in size must have profoundly influenced the thermodynamic role played by the Global Warm Pool. The central portion of the SCS experienced a considerable decline in the sea-surface temperature (SST) during the LGM. The winter monsoon strengthened, the polar front shifted southward, and the Kuroshio Current migrated eastward. All of these changes caused a drastic decrease in the winter SST in the Western Pacific marginal seas in general and in the SCS particularly (Wang and Wang, 1990; Miao et al., 1994; Wang et al., 1995b). Together with the negligible changes in the summer SST, the decrease in winter SST resulted in a much more intensive seasonality during the LGM (Fig. 7B; Wang, in press). Among the important consequences of the glacial changes of the SCS is the intensified aridity in China. The SCS is the main source of water vapor for precipitation in East China (Chen et al., 1991). The above-described shelf emergence and SST decline must have led to a reduction in evaporation and vapor supply from the sea to the land. A very preliminary estimate shows that the reduction in evaporation from the SCS during the LGM could correspond to 1/8 to 1/4 of the annual precipitation in all of China (Wang et al., 1997). The glacial reduction in vapor supply from the sea at least partially explains the intensification of aridity in the China hinterland as evidenced, for example, by the extensive distribution of loess deposits. Moreover, the glacial increase of seasonality in the marginal seas may offer an alternate approach to the tropical paleoclimate enigma in the Pacific, that is, the discrepancy between marine and terrestrial indicators of paleotemperature during the LGM (Stuijts et al., 1988; Andersen and Webb, 1994). The late Quaternary studies have demonstrated the great potential of the SCS's hemipelagic sediments to provide high-resolution paleoenvironment records. A core from the northern SCS (SONNE 17940) reveals a highly detailed transition from glacial to Holocene conditions (Wang et al., in press). On the basis of low fluvial clay content (50%-60%) and high modal grain size (10-25 æm) during the LGM and stage 3 and the transition to high clay content (>70%) and low modal grain size (<6.3 æm) in the Holocene (Fig. 8), a strong winter monsoon and weak summer monsoon precipitation are inferred for the glacial regime and a strong summer monsoon and weakened winter monsoon are inferred for the Holocene regime. The d18O data from the mixed layer planktonic foraminifer Globigerinoides ruber reveal numerous short-term light d18O events superimposed on the main pattern of glacial-postglacial change (Fig. 8). These events are interpreted to reflect increases in summer monsoon intensity, i.e., reduced sea-surface salinity together with increases of fluvial clay and decreases in modal grain size. The increases in summer monsoon intensity can be correlated with Dansgaard-Oeschger events 1-10 in the GISP2 ice core (Fig. 8). Also observed in this SCS core are four periods of relatively heavy d18O associated with low fluvial clay content and high grain size, i.e., reduced summer monsoon precipitation and increased winter monsoon wind, which correlate to the Heinrich events 1-4 (Fig. 8). The early Holocene/Pre Boreal (EHPB) summer monsoon maximum revealed by a broad d18O minimum and fluvial clay maximum has also been reported from the Arabian Sea (Prell, 1984b; Sorocko, et al., 1993). The 8.2k cooling event recorded in the GISP2 ice core appears to coincide with a large increase in d18O and hence decrease in summer monsoon precipitation in the SCS. The Leg 184 cores, along with the recent cores from the joint German-Chinese expedition Monitor Monsoon (Sarnthein et al., 1994), and the IMAGES III Cruise in 1997 provide for the first time systematic and high-quality material for paleomonsoon studies in the region (e.g., Wang et al., 1995a; Sun, 1996; Sun and Li, in press). SCIENTIFIC OBJECTIVES The long-term goals of Leg 184 are to determine the evolution and variability of the East Asian monsoon during the late Cenozoic and to improve our knowledge of the links between climate and tectonics. To meet these goals, Leg 184 has a number of major cruise and shore-based scientific objectives, including the following (1) Obtain continuous sequences of hemipelagic sediments that record the East Asian climate history during the late Cenozoic. The drilling plan takes advantage of the high hemipelagic sedimentation rates in the SCS to recover sections that are suitable for high-resolution stratigraphy. The seismic surveys reveal that different areas of the northern slope contain expanded sections of different ages. Our shipboard objective (see Proposed Sites and Operational/Drilling Plan sections) is to recover complete, high- accumulation rate sections for each age interval. For example, sedimentation rates on the continental slope vary from 0.7 to 15 cm/k.y. for the Holocene and from 1.3 to 31 cm/k.y. for the LGM, with the maximum values found near the mouth of the Pearl River and the paleo-Sunda River (Wang et al., 1995b). Recently, Core 17940 (20¡07N, 117¡23E, in a water depth of 1727 m; Sarnthein et al., 1994) in the northeast SCS, revealed a Holocene section nearly 7 m in thickness, which enables a temporal resolution of less than 15 yr (Fig. 8). The proposed drilling during Leg 184 will provide continuous records of monsoon variations back to the late Paleogene, enabling a comparison with the Indian monsoon records. (2) Establish records of monsoonal proxies for the SCS, including the variability of sediment properties, the rates of sediment accumulation, and the chemical, isotopic, and species variability of flora and fauna. On the basis of previous studies we anticipate that a number of sediment properties will exhibit variability related to monsoonal forcing (Figs. 3, 7, 8). Shipboard measurements will include core logging of magnetic susceptibility, bulk density, color reflectance, and natural gamma radiation, which along with faunal variations, can be related to monsoonal climates. Much of the previously identified monsoonal variability in tropical oceans is precessional (23 k.y.) in scale. We will construct initial splices and age models to identify the primary periodicity of the SCS records. By inference, strong precessional responses are likely related to monsoonal processes. Postcruise work will measure and refine the time series of chemical, isotopic, and faunal variability to give additional constraints on the relationship between sediment proxies and monsoonal variability. (3) Establish stratigraphic ties between the SCS marine record and the terrestrial record of China. Petroleum exploration and academic studies have accumulated a tremendous amount of Cenozoic paleoenvironmental information, particularly for on land and offshore China (Fig. 6). Because of the language barrier and commercial restrictions, little of these data have been available to the global scientific community. In addition, the poor stratigraphic control of the mostly nonmarine deposits has made it difficult to correlate the sediment records with the global paleoenvironmental history. The shipboard stratigraphy of the proposed sites will provide the first direct calibration of open-marine stratigraphy to the local and regional land-based stratigraphies, thereby linking them with the record of global environmental changes. Special attention will be paid to the timing of drastic changes in denudation/accumulation, monsoon intensification, seasonal cooling, and to the leads or lags between terrestrial and marine records. (4) Establish the relationship of East Asian monsoon variability with orbital and glacial forcing, and internal feedbacks of the climate system. The variability of monsoonal proxies and sedimentary characteristics identified on shipboard and in postcruise studies will be compared directly to time series of orbital changes to establish their coherency and phase (Fig. 3). Initial shipboard results should establish if the SCS monsoonal variations are consistent with orbital models of monsoonal variability. Postcruise research will be needed to expand and refine the sedimentary time series and perform more rigorous tests. (5) Compare the evolution of the East Asian monsoon in the SCS with the Indian monsoon in the Arabian Sea to identify common sources of causality. Given the identification of monsoonal indices in the SCS, especially for the winter monsoon, the SCS records will be compared to records of the summer monsoon from the ODP Arabian Sea sites. We anticipate that the summer monsoon signals should be similar (in phase) and that the winter monsoon will be stronger in the SCS. Since the winter monsoon reflects cooling over northern Asia, which is a function of both precession and obliquity, it may exhibit a more complex response than the summer monsoon. These studies will be initiated on shipboard, but most detailed comparisons will be made only after the final time series are established by postcruise research. (6) Test scenarios for the relationship between the Tibetan Plateau uplift, monsoon evolution, and global cooling. Land-based studies in China and marine-based ODP studies have postulated a variety of models for monsoon evolution (Table 1; Figs. 3, 4). The proposed drilling and logging program will calibrate the terrestrial records with those of the global ocean and make use of monsoonal proxies to establish the history of monsoon evolution in the SCS. Because uplift of the Tibetan Plateau is proposed to be responsible for both the late Cenozoic global cooling and for the intensification of the Asian monsoon, a comparison between records of monsoon intensity, denudation/accumulation rates, and climate cooling in the SCS will help test these hypotheses. However, the relationships between tectonics, erosion, and climate are complex and highly nonlinear (see papers in Ruddiman, 1997). The tectonic control of the Asian monsoons, for example, is by no means limited to the plateau uplift. Only recently has the marine factor for monsoon evolution been discussed, but then only the role of the Paratethys was considered (Ramstein et al., 1997); whereas, the Western Pacific marginal seas should have more direct impact on the evolution of the East Asian monsoon. Drilling in the SCS will allow insights into the mechanisms of monsoon variation and will provide a new set of constraints concerning the links between tectonic uplift, weathering/erosion, and climate. The shipboard identification of sediment characteristics and accumulation rates in the Miocene to Pleistocene sections of the SCS will likely distinguish between some models of monsoon evolution but will also raise questions or present new patterns to be deciphered. Significant postcruise research will be directed toward determining how the various sedimentary records are related to the models of HTC uplift and global cooling. (7) Improve our understanding of seasonality in the low-latitude SCS and how it relates to the strength and evolution of the winter monsoon. Late Neogene sections from the northern and southern part of the SCS will enable us to construct a history of the thermal gradient within the SCS (Fig. 7B). These paleotemperature data will provide information on when the winter monsoon began to develop large seasonality in the SCS and on the stability/variability of temperatures in the southern SCS, which lies within the Western Pacific Warm Pool. Although seasonality is not necessarily related to monsoon circulation, intensification of monsoon circulation can trigger an increase in seasonality. The glacial increase in seasonality within the SCS is at least partly attributed to the strengthening of the East Asian winter monsoon. Aside from SST estimates, seasonality can also be recognized through abundance of index species in planktonic fauna. PROPOSED SITES Six primary and two alternate sites are proposed for drilling (Table 2). These fall into two groups: northeastern continental slope (Fig. 9) and southern slope (Fig. 10). A summary of the water depths for each site and the expected age/penetration is given in Figure 11. 1. Northeastern Continental Slope Sites SCS-1 to 5 are located south of the Dongsha Islands in the northeast SCS (Fig. 9). The sites are designed to sample different water depths and to cover successive time intervals since the Oligocene (SCS-1: Pleistocene; SCS-2: middle Pliocene onward; SCS-3: Pliocene and Pleistocene; SCS-4: middle Miocene to Pliocene; SCS-5: Oligocene to Miocene). This suite of sites should provide the sections to identify and date the proposed stages of monsoon evolution in East Asia. Site SCS-1 SCS-1 is targeted for 2050 m water depth, which is slightly above the sill depth of the Bashi Straits (2600 m). The location of Site SCS-1 is distinguished by extremely high sedimentation rates. The Holocene deposits in the nearby Core 17940 (20¡07N, 117¡23E, water depth 1727 m) reach almost 7 m in thickness, and Core MD 97.2.146 extends only to the oxygen stage 4/5 boundary at 38 m (C.Y. Huang, pers. comm., 1997). The summer monsoon cyclicity of 102 yr in the Holocene and the dry/humid cyclicity of 103 yr in the late Pleistocene found in Core 17940 (Wang et al., 1995a; Sun, 1996) indicate the great potential of this site in delivering high-resolution monsoon records for the Pleistocene. The target penetration of 450 m is anticipated to recover Quaternary sediments (~1 m.y.). Site SCS-2 Proposed Site SCS-2 is downslope of SCS-1 at a water depth of 3190 m. This location has a lower sedimentation rate and is expected to provide a continuous record from the middle Pliocene to Pleistocene (Holocene). Because the sill depth of the Bashi Strait is located at ~2600 m, Sites SCS-1 and SCS-2 will also document the Quaternary changes in water mass characteristics across the sill, which is the only deep-water connection between the Pacific and the SCS. SCS-2 is targeted for 400 m penetration. Site SCS-3C Site SCS-3C is on the upper slope (water depth ~1265 m) near the base of the modern oxygen minimum zone (State Oceanic Administration, 1988; Haupt et al., 1994). This site is expected to provide a sequence of Pliocene and Pleistocene sediments that record changes in the intermediate water characteristics well above the sill depth. The variables of most interest are temperature and oxygen content, as well as surface-water conditions. Site SCS-3C is targeted for 300 m penetration. Site SCS-4 Site SCS-4 is downslope of Site SCS-3C at a water depth of 2093 m. On the basis of seismic records, the proposed site should recover a middle Miocene to Pliocene sequence, which underlies relatively thin Pleistocene deposits. This site also lies above the current sill depth of the Bashi Straits and, along with SCS-5C, offers a Mio-Pliocene history of sill-related water-mass changes. SCS-4 is targeted for 520 m penetration. Site SCS-5C Site SCS-5C is located lower on the slope (3232 m) and is expected to recover an expanded Oligocene to Miocene section. On the basis of available seismic records and their correlation to Chinese reflector stratigraphy, SCS-5C is targeted for 700 m penetration. Given the expected accumulation rates and penetration depths, SCS-5C (and the alternate SCS-5D) are the only sites that will recover the Oligocene-Miocene history of the SCS, including the possible onset of the East Asian monsoon. Alternate Sites SCS-5D and SCS-5E Sites SCS-5D and SCS-5E are located about 65 and 20 km, respectively, northeast of Site SCS- 5C. These alternate sites provide a somewhat expanded midsection compared to SCS-5C. They could be cored, if SCS-5C does not meet the expectations of a complete Oligocene-Miocene section. 2. Southern Slope A southern continental slope SCS site is proposed to reveal the history of tropical East Asia and the Western Pacific Warm Pool (Fig. 10). Although the terrigenous deposits of the paleo-Sunda and Mekong Rivers provide a number of attractive targets in the southern part of the SCS, and piston cores in the region have high sedimentation rates and display high frequency climate variations, especially since the last glaciation. Safety considerations have entailed moving the site farther downslope (to the north) and limiting penetration. This southern location will be the only site within the Western Pacific Warm Pool and will provide a thermal contrast to the northern sites. Site SCS-9 Proposed Site SCS-9 is at a water depth of 2830 m. Penetration is limited to 400 m, reaching the upper part of the upper Miocene. OPERATIONAL/DRILLING STRATEGY A number of operational, practical, and strategic factors were considered when developing the operational plan for Leg 184. Briefly, these include 1.Sites were selected to maximize recovery of different stratigraphic sections and different water depths. The northern continental margin sites comprise two transects: an eastern pair of sites that will focus on the Plio-Pleistocene section (Sites SCS-1 and SCS-2) at 2050 and 3190 m, respectively, and a western pair of sites that will focus on the Oligocene to Miocene section (Sites SCS-4 and SCS-5C) at 2093 and 3250 m, respectively. 2.All sites are considered to be first priority, but Site SCS-3C is considered at risk if operational time is limited. Site SCS-5C is considered to be the highest priority as it is the only site that will recover the Oligocene to Miocene section of the SCS. Alternate Site SCS- 5D or 5E may become a higher priority than SCS-3C, if the coring results at SCS-5C do not satisfactorily recover the early history of the monsoon. 3.All sites will be triple piston cored (advanced hydraulic piston core [APC]) and extended core barrel (XCB) cored to total depth, with the possibility of double XCB if critical sections are not adequately recovered. The deeper sections of Site SCS-5C may be cored with the rotary core barrel system (RCB), if XCB penetration and recovery are not adequate. 4.Because of the limited number of seismic crossing lines at proposed sites, the JOIDES Resolution will conduct a seismic reflection survey (~2 to 2.5 days at Sites SCS-2, 3C, 4, and 5C and, if required, Sites SCS-5D and 5E) to verify that the proposed sites are safe and to provide a better structural framework for interpreting the sediment accumulation patterns. Coring at all but SCS-1 is contingent on safety panel approval, which will be based on the survey data. 5.Taking the above operational/coring considerations into account, the following sequence of operations is proposed: Depart Freemantle and transit to proposed Site SCS-9 and core. Then transit to Site SCS-1 and core. We will then conduct a seismic survey of northern sites to collect cross lines and select final site locations. Following the survey, we anticipate coring proposed Sites SCS-2, SCS-5C (or alternate), SCS-4, and SCS-3C in sequence before the final transit to Hong Kong. 6.ODP has requested Exclusive Economic Zone (EEZ) clearance for all proposed sites. Site SCS-9 requires drilling in waters that are claimed by several nations and EEZ clearance of this site may therefore be more problematic than for the northern sites. If SCS-9 should not get approved, the remaining time will be used to achieve the objectives, and maximize recovery, at the other sites, including SCS-3C. WIRELINE LOGGING PLAN The Leg 184 logging plan has been designed to provide (1) complete stratigraphic coverage, especially useful if core recovery is incomplete; (2) proxy data not available from core measurements, such as resistivity and yields of K, U, and Th; and (3) in situ sonic velocity for the construction of synthetic seismograms. All sites drilled to a depth greater than 400 m will be logged using the following three tool strings (see: http://www.ldeo.columbia.edu/BRG/ new_kiosk.html for additional information on the tools): A. "Triple-combo" toolstring, which includes: (1) the Dual Induction Tool (DITE) that measures resistivity from deep and shallow induction; (2) the Accelerator Porosity Sonde (APS) to measure porosity from epithermal neutron measurements; and (3) the Hostile Environment Litho-Density Sonde (HLDS) that measures bulk density from Compton scattering and general lithology from the photoelectric effect. The Hostile Environment Natural Gamma Ray Sonde (HNGS) that measures total natural gamma radiation and K, U, Th yields, and the LDEO Temperature Logging Tool (TLT) that measures borehole fluid temperature, are added to this toolstring. B. "FMS-Sonic" toolstring which includes (1) the Formation Microscanner (FMS) that includes the General Purpose Inclinometry Tool (GPIT) and measures micro-resistivity at cm resolution; (2) the Dipole Sonic imager (DSI) that measures compressional and shear wave velocity, as well as cross dipole and Stoneley waveforms. C. Geologic High-resolution Magnetic Tool (GHMT), which includes the Nuclear Magnetic Remanence Sonde (NMRS) to measure the total magnetic field, and the Susceptibility Measurement Sonde (SUMS) to measure the magnetic susceptibility from induction. All tool names are trademarks of Schlumberger, except the TLT. Use of the FMS-Sonic and GHMT toolstrings is contingent on hole conditions as estimated from the caliper measurements with the triple-combo string (always used for the first run), and the general course of the previous logging run. Estimated logging times for all three runs vary from 28 to 38 hr for the each of the Leg 184 sites. SAMPLING STRATEGY AND SAMPLING PLAN General Sampling of the recovered cores will be subject to the rules described in the ODP Sample Distribution Policy (http://www-odp.tamu.edu/curation/sdp.htm). Based on the sample requests received by 15 November 1998, the Sample Allocation Committee (SAC) will prepare a temporary sampling plan, to be revised on the ship according to actual coring results. In the final shipboard sampling plan, sample requests will be closely linked to proposed postcruise research. Postcruise studies can also be proposed by shore-based investigators who do not participate in the cruise. Logistics The core sampling logistics are three-fold: (1) shipboard sampling for shipboard measurements, (2) shipboard sampling for postcruise studies, and (3) postcruise sampling for postcruise studies. Some sampling for shipboard measurement of ephemeral properties must occur immediately, before stratigraphic correlation information is available (see below). These measurements include organic geochemistry for safety monitoring (free gas and 20 cm3 sediment samples), interstitial- water chemistry (whole-round of 5-15 cm length), and moisture content (10 cm3 sediment). In addition, core catchers will be analyzed for biostratigraphic datums. Shipboard sampling for postcruise studies will be kept to a reasonable minimum, trying to balance the need for an initial set of samples for immediate postcruise laboratory work against the need for avoiding redundant or "frenzy" sampling before the composite section and splice are constructed (see below). The SAC may decide to sample the upper few cores on the ship because high- porosity sediments could be disturbed during transport to the Texas A&M University (TAMU) core repository. Samples that need to be frozen or sealed for shore-based analysis also must be taken onboard. All shipboard scientists will participate in shipboard sampling according to a shift schedule. Because of the large number of requested samples that are expected, most investigators will be encouraged to participate in a postcruise sampling meeting in the core repository ~4 months postcruise. The ODP repository staff will fill the remaining requests. Core Material Most of the material to be recovered is expected to be hemipelagic mud with moderate carbonate content and low abundance of organic material. Sedimentation rates are expected to range typically between 2-20 cm/k.y., although some sites may have substantially higher rates. Stratigraphic Coverage, MCD, and the Splice Complete stratigraphic coverage will be attempted at all sites. Because coring gaps occur, even between successive cores with nominally 100% recovery, complete sections will be achieved by triple coring with the APC system (typically the uppermost 150-250 m). Double XCB coring of the deeper intervals may be considered, depending on the priority of the section and the available time. In addition to ensuring complete coverage, multiple-hole coring also provides significantly more core material for sampling. The shipboard stratigraphic correlators will be responsible for constructing a composite depth section for each site in near-real time. The "meters composite depth" (mcd) scale correlates the cores from multiple holes based on core logging data. All investigations from any hole can then be linked by using the mcd scale. 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Carbonate sedimentation cycles in the northern South China Sea during the late Quaternary. In Zheng, L., and Chen, W. (Eds.), Contributions to Sedimentation Process and Geochemistry of the South China Sea. China Ocean Press, 109-123 (in Chinese, with English abstract). SITE SUMMARIES Site: SCS-1 Priority: 1 Position: 20¡03.18'N, 117¡25.14'E Water Depth: 2050 m Sediment Thickness: ~760 m Approved Maximum Penetration: 450 m Seismic Coverage: Intersection of SO-95 Profiles 10 and 20 Objectives 1.To recover a continuous sequence of high accumulation rate hemipelagic sediments to reconstruct the Pleistocene paleomonsoon history on a millenial (or higher resolution) time scale. 2.To identify the time scales of variability for sediment characteristics and accumulation rates. The time series of sediment variability will be compared with records of orbital-scale and higher frequency records from ice cores, marginal seas, and terrestrial deposits. 3.To establish a high-resolution record of SST changes associated with the winter monsoon and for comparison to the SST history of the southern SCS. Drilling Program: Triple APC to refusal, XCB to 450 mbsf Logging and Downhole Operations: Triple-combo, GHMT, and sonic-FMS Nature of Rock Anticipated: Hemipelagic mud Site: SCS-2 Priority: 1 Position: 19¡35.04'N, 117¡37.86'E Water Depth: 3190 m Sediment Thickness: ~870 m Approved Maximum Penetration: 400 m Seismic Coverage: Intersection of SO-95 Profile 10 and Vema Profile 3068 Objectives: 1.To recover a continuous sequence of hemipelagic sediments to reconstruct the middle Pliocene to Pleistocene/Holocene paleomonsoon history. 2.To establish if the SCS records an intensification of the winter monsoon during the Pliocene, consistent with the development of loess in China. 3.To establish if the summer monsoon is intensifying or weakening during the Plio- Pleistocene. Drilling Program: Triple APC to refusal, XCB (or double XCB) to 400 mbsf Logging and Downhole Operations: Triple-combo, GHMT, and sonic-FMS Nature of Rock Anticipated: Hemipelagic mud and mudstone Site: SCS-3C Priority: 1 Position: 19¡ 59.76'N, 116¡0.90'E Water Depth: 1265 m Sediment Thickness: 810 m Approved Maximum Penetration: 300 m Seismic Coverage: Intersection of SO-95 Profile 5 and SO-72A Profile 18 Objectives: 1.To recover a continuous sequence of hemipelagic sediments to reconstruct the late Miocene (?) to Pleistocene paleomonsoon history. 2.To determine the characteristics and variability of upper slope sediments bathed in intermediate waters, possibly with low oxygen content. 3.To provide the shallow end-member (1265 m) for the Plio-Pleistocene depth transect to examine the vertical gradients of water mass properties and carbonate preservation. Drilling Program: Single APC to refusal, XCB to 300 mbsf Logging and Downhole Operations: None Nature of Rock Anticipated: Hemipelagic mud and silt seismic SCS-4 Site: SCS-4 Priority: 1 Position: 19¡27.24'N, 116¡15.84'E Water Depth: 2093 m Sediment Thickness: 1400 m Approved Maximum Penetration: 520 m Seismic Coverage: Intersection of SO-95 Profile 5 Objectives: 1.To recover a continuous sequence of hemipelagic sediments to reconstruct the middle Miocene to Pliocene paleomonsoon history. 2.To identify if monsoonal indices intensify or weaken during the middle to late Miocene as a test of monsoon evolution models. 3.To establish if Miocene-Pliocene pattern of accumulation rates are consistent with models of HTC uplift, monsoon intensification, and sea-level changes. Drilling Program: Triple APC to refusal, XCB (possibly double XCB) to 520 mbsf Logging and Downhole Operations: Triple-combo, GHMT, and sonic-FMS Nature of Rock Anticipated: Hemipelagic mud and silt Site: SCS-5C Priority: 1 Position: 18¡49.73'N, 116¡32.93'E Water Depth: 3232 m Sediment Thickness: 750 m Approved Maximum Penetration: 700 m Seismic Coverage: SO-95 Profile 5 near intersection with Profile 20 Objectives: 1.To recover a continuous sequence of hemipelagic sediments to reconstruct the paleoclimate history from Oligocene to Miocene. 2.To identify the onset of monsoonal variability in the SCS and to establish its evolution in the Oligo-Miocene interval. 3.To establish if Oligo-Miocene pattern of accumulation rates are consistent with models of HTC uplift, monsoon intensification, and sea-level changes. Drilling Program: Triple APC to refusal, XCB (possibly double XCB) to 450 m, RCB to 700 m Logging and Downhole Operations: Triple-combo, GHMT, and sonic-FMS Nature of Rock Anticipated: Hemipelagic mud and silt Site: SCS-5D Priority: 1 Position: 19¡20.94'N, 116¡51.66'E Water Depth: 2682 m Sediment Thickness: 1160 m Approved Maximum Penetration: 700 m Seismic Coverage: SO-95 Profile 20 Objectives: 1.To recover a continuous sequence of hemipelagic sediments to reconstruct the paleoclimate history from Oligocene to Miocene. 2.To identify the onset of monsoonal variability in the SCS and to establish its evolution in the Oligo-Miocene interval. 3.To establish if Oligocene-Miocene pattern of accumulation rates are consistent with models of HTC uplift, monsoon intensification, and sea-level changes. Drilling Program: Triple APC to refusal, XCB (possibly double XCB) to 450 m, RCB to 700 m Logging and Downhole Operations: Triple-combo, GHMT, and sonic-FMS Nature of Rock Anticipated: Hemipelagic mud and silt Site: SCS-5E Priority: 1 Position: 19¡0.36'N, 116¡35.88'E Water Depth: 3143 m Sediment Thickness: 1160 m Approved Maximum Penetration: 770 m Seismic Coverage: SO-95 Profile 20 Objectives: 1.To recover a continuous sequence of hemipelagic sediments to reconstruct the paleoclimate history from Oligocene to Miocene. 2.To identify the onset of monsoonal variability in the SCS and to establish its evolution in the Oligocene-Miocene interval. 3.To establish if Oligocene-Miocene pattern of accumulation rates are consistent with models of HTC uplift, monsoon intensification, and sea-level changes. Drilling Program: Triple APC to refusal, XCB (possibly double XCB) to 450 m, RCB to 770 m Logging and Downhole Operations: Triple-combo, GHMT, and sonic-FMS Nature of Rock Anticipated: Hemipelagic mud and silt Site: SCS-9 Priority: 1 Position: 09¡21.72'N, 113¡17.10'E Water Depth: 2830 m Sediment Thickness: 1010 m Approved Maximum Penetration: 400 m Seismic Coverage: Intersection of lines NS95-240 and NSL95-160 Objectives: 1.To recover a continuous sediment record to reconstruct the paleoclimate history in the tropical SCS during the late Neogene. 2.To determine variations in the supply of terrigenous sediment from the Mekong and southern sources. 3.To establish the record of SST variability in the SCS as a measure of the Western Pacific Warm Pool and for comparison to the seasonal SST patterns of the northern SCS. Drilling Program: Triple APC to refusal, XCB to 400 mbsf Logging and Downhole Operations: Triple-combo, GHMT, and sonic FMS Nature of Rock Anticipated: Hemipelagic mud, silt, and other clastic sediments and rocks SCIENTIFIC PARTICIPANTS Co-Chief Warren L. Prell Department of Geological Sciences Brown University Box 1846 Providence, RI 02912 U.S.A. Internet: warren_prell@brown.edu Work: (401) 863-3221 Fax: (401) 863-2058 Co-Chief Pinxian Wang Department of Marine Geology and Geophysics Tongji University Shanghai 200092 People's Republic of China Internet: pxwang@online.sh.cn Work: (86) 21-6598-3207 Fax: (86) 21-6513-8808 Staff Scientist Peter Blum Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: peter_blum@odp.tamu.edu Work: (409) 845-9299 Fax: (409) 845-0876 Inorganic Geochemist Christophe J. G. Colin Laboratoire de Geochemie des Roches Sedimentaires Universite de Paris-Sud XI BAT. 504 Orsay Cedex 91405 France Internet: colin@geol.u-psud.fr Work: (33) 1-69-15-67-45 Fax: (33) 1-69-15-48-82 Inorganic Geochemist Katherine McIntyre Marine Sciences Institute University of California, Santa Barbara Santa Barbara, CA 93106 U.S.A. Internet: mcintyre@lifesci.ucsb.edu Work: (805) 893-7061 Fax: (805) 893-8062 Organic Geochemist Matthew J. Higginson School of Chemistry University of Bristol Cantock's Close Bristol BS8 1TS United Kingdom Internet: matthew.higginson@bristol.ac.uk Work: (44) 117-928-9000, ext 4430 Fax: (44) 117-929-3746 Organic Geochemist Joel S. Leventhal Private Consultant: U.S.A. Diversified Geochemistry 8944 W. Warren Dr. Lakewood, CO 80227 U.S.A. Internet: hoflev@aol.com Work: (303) 988-7269 Fax: JOIDES Logging Scientist Jian Lin Department of Geology and Geophysics Woods Hole Oceanographic Institution Woods Hole, MA 02543 U.S.A. Internet: jlin@whoi.edu Work: (508) 289-2576 Fax: (508) 457-2187 Paleomagnetist Carlo E. Laj Laboratoire des Sciences du Climat et de l'Environnement (LSCE) CNRS Bat. 12 Avenue de la Terrasse Gif-sur-Yvette Cedex 91198 France Internet: laj@lsce.cnrs-gif.fr Work: (33) 1-69-82-35-38 Fax: (33) 1-69-82-35-68 Paleomagnetist Peter A. Solheid Institute for Rock Magnetism University of Minnesota, Minneapolis 287 Shepherd Laboratories Minneapolis, MN 55455-0128 U.S.A. Internet: peat@umn.edu Work: (612) 624-5274 Fax: (612) 625-7502 Paleontologist (Foraminifer) Zhimin Jian Department of Marine Geology and Geophysics Tongji University Siping Road 1239 Shanghai 200092 People's Republic of China Internet: zjiank@online.sh.cn Work: (86) 21-6598-3207 Fax: (86) 21-6513-8808 Paleontologist (Foraminifer) Stephen A. Nathan Department of Geosciences University of Massachusetts Morrill Science Center Amherst, MA 01003 U.S.A. Internet: snathan@geo.umass.edu Work: (413) 545-2016 Fax: (413) 545-4884 Paleontologist (Nannofossil) Jih-Ping Shyu Institute of Oceanography National Taiwan University P.O. Box 23-13 Taipei 10617 Taiwan Internet: jpshyu@iodec1.oc.ntu.edu.tw Work: (886) 2-391-4442 Fax: (886) 2-391-4442 Paleontologist (Nannofossil) Xin Su Department of Geology China University of Geosciences Xueyuan Road 29 Beijing 100083 People's Republic of China Internet: xsu@sky.cugb.edu.cn Work: (86)10-62312244-2261 Fax: (86)10-62937940 Physical Properties Specialist Christian J. Buhring Geologisch-Palaontologisches Institut Christian-Albrechts-Universitat zu Kiel Olshausenstrasse 40 Kiel 24118 Federal Republic of Germany Internet: cb@zaphod.gpi.uni-kiel.de Work: (49) 431-880-2966 Fax: (49) 431-880-4367 Physical Properties Specialist Min-Pen Chen Institute of Oceanography National Taiwan University P.O. Box 23-13 Taipei 10617 Taiwan Internet: minpen@ccms.ntu.edu.tw Work: (886) 2-2391-4442 Fax: (886) 2-2364-4049 Sedimentologist Eve M. Arnold Geologi och Geokemi Stockholms Universitet Stockholm 106 91 Sweden Internet: emarnold@geo.su.se Work: (46) 867-47598 Fax: (46) 867-47897 Sedimentologist Peter D. Clift Department of Geology and Geophysics Woods Hole Oceanographic Institution MS#22 Woods Hole, MA 02543 U.S.A. Internet: pclift@whoi.edu Work: (508) 289-3437 Fax: (508) 457-2187 Sedimentologist Wolfgang Kuhnt Geologisch-Palaontologisches Institut Christian-Albrechts-Universitat zu Kiel Olshausenstrasse 40 Kiel 24118 Federal Republic of Germany Internet: wk@gpi.uni-kiel.de Work: (49) 431-880-2924 Fax: (49) 431-880-4376 Sedimentologist Anchun Li Institute of Oceanology Chinese Academy of Sciences 7 Nanhai Road Qingdao, Shandong Province 266071 People's Republic of China Internet: acli@ms.qdio.ac.cn Work: (86) 532-287-9062, ext 2214 Fax: (86) 532-287-0882 Sedimentologist Federica Tamburini Insitute de G‚ologie Universit‚ de Neuchƒtel Rue Emile Argand, 11 Neuchƒtel 2007 Switzerland Internet: federica.tamburini@geol.unine.ch Work: (41) 32-718-26-20 Fax: (41) 32-718-26-01 Sedimentologist Alain Trentesaux Laboratoire de Sedimentologie et Geodynamique Universite de Lille I SN5 Villeneuve d'Ascq Cedex 59655 France Internet: alain.trentesaux@univ-lille1.fr Work: (33) 3-20-43-49-10 Fax: (33) 3-20-43-49-15 Sedimentologist Luejiang Wang Graduate School of Environmental Earth Science Hokkaido University Nishi 5 Kita 10 Kita Ku Sapporo 060-0810 Japan Internet: ljwang@ees.hokudai.ac.jp Work: (81) 11-706-5303 Fax: (81) 11-736-3290 Stratigraphic Correlator Steven C. Clemens Department of Geological Sciences Brown University Box 1846 Providence, RI 02912-1846 U.S.A. Internet: steven_clemens@brown.edu Work: (401) 863-1964 Fax: (401) 863-2058 Stratigraphic Correlator John W. Farrell Joint Oceanographic Institutions Inc. 1755 Massachusetts Ave. NW Suite 800 Washington, DC 20036-2102 U.S.A. Internet: jfarrell@brook.edu Work: (202) 232-3900 Fax: (202) 232-8203 LDEO Logging Scientist Christine Lauer Laboratoire de Geochimie Isotopique Universite Montpellier II ISTEEM Case 066 - Place Eugene Bataillon Montpellier Cedex 05 34095 France Internet: christine.lauer-leredde@dstu.univ-montp2.fr Work: (33) 4-42-97-11-33 Fax: (33) 4-42-97-11-21 LDEO Logging Trainee Qingmou Li Institute of Geophysics Chinese Academy of Sciences P.O. Box 9701 A-11 Datun Road Beijing 100101 People's Repubilc of China Internet: qmlee@c-geos15.c-geos.ac.cn Work: Fax: (86) 10-6487-1995 Schlumberger Engineer Robert Laronga Schlumberger Offshore Services 369 Tristar Drive Webster, TX 77598 U.S.A. Internet: laronga@webster.wireline.slb.com Work: (281) 480-2000 Fax: (281) 480-9550 Operations Manager Ron Grout Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: ron_grout@odp.tamu.edu Work: (409) 845-2144 Fax: (409) 845-2308 Laboratory Officer Kuro Kuroki Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: kuro_kuroki@odp.tamu.edu Work: (409) 845-8482 Fax: (409) 845-0876 Marine Lab Specialist: Yeoperson Michiko Hitchcox Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: michiko_hitchcox@odp.tamu.edu Work: (409) 845-2483 Fax: (409) 845-0876 Marine Lab Specialist: Chemistry Dennis Graham Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: dennis_graham@odp.tamu.edu Work: (409) 845-8482 Fax: (409) 845-0876 Marine Lab Specialist: Chemistry Chieh Peng Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: chieh_peng@odp.tamu.edu Work: (409) 845-2480 Fax: (409) 845-0876 Marine Lab Specialist: Core Maniko Kamei Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: maniko_kamei@odp.tamu.edu Work: Fax: Marine Lab Specialist: Curator Gerald Bode Scripps Institution of Oceanography University of California, San Diego Ocean Drilling Program West Coast Repository La Jolla, CA 92093-0231 U.S.A. Internet: gerald_bode@odp.tamu.edu Work: (619) 534-1657 Fax: Marine Lab Specialist: Assistant Curator Peter Esmay Lamont-Doherty Earth Observatory Columbia University ODP East Coast Repository Route 9W Palisades, NY 10964 U.S.A. Internet: peter.esmay@odp.tamu.edu Work: (914) 365-8446 Fax: (914) 365-8178 Marine Lab Specialist: Downhole Tools, Marine Lab Specialist: Thin Sections Gus Gustafson Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: ted_gustafson@odp.tamu.edu Work: (409) 845-8482 Fax: (409) 845-0876 Marine Lab Specialist: Paleomagnetics Charles A. Endris Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845 U.S.A. Work: (409) 845-5135 Fax: (409) 845-0876 Marine Lab Specialist: Photographer Tim Fulton Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A Internet: tim_fulton@odp.tamu.edu Work: (409) 845-1183 Fax: (409) 845-4857 Marine Lab Specialist: Physical Properties Anastasia Ledwon Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: anastasia_ledwon@odp.tamu.edu Work: (409) 845-9186 Fax: (409) 845-0876 Marine Lab Specialist: Underway Geophysics Don Sims Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: don_sims@odp.tamu.edu Work: (409) 845-2481 Fax: (409) 845-0876 Marine Lab Specialist: X-Ray Robert Olivas Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: bob_olivas@odp.tamu.edu Work: (409) 845-2481 Fax: (409) 845-0876 Marine Lab Specialist: Marine Logistics Coordinator Larry Obee Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: larry_obee@odp.tamu.edu Work: (409) 862-8717 Fax: (409) 845-2380 Marine Electronics Specialist Randy W. Gjesvold Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station , TX 77845-9547 U.S.A. Internet: randy_gjesvold@odp.tamu.edu Work: Fax: Marine Electronics Specialist Larry St. John Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: larry_st.john@odp.tamu.edu Work: (409) 845-2454 Fax: (409) 845-2308 Marine Computer Specialist Mike Hodge Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: mike_hodge@odp.tamu.edu Work: (409) 862-4845 Fax: (409) 845-4857 Marine Computer Specialist David Kotz Ocean Drilling Program Texas A&M University 1000 Discovery Drive College Station, TX 77845-9547 U.S.A. Internet: david_kotz@odp.tamu.edu Work: (409) 862-4848 Fax: (409) 845-4857