Correlation of the logs from the Izu-Bonin forearc sedimentary sections at Sites 787, 792, and 793 with the core data from Holes 787A-787B, 792A-792E, and 793A-793B allows the development of a more detailed lithostratigraphic model for those sites, and a more precise correlation of lithologic boundaries to basin-wide seismic reflections. Early Oligocene arc volcanics form the basement strata (Unit 5) sampled at Sites 792 and 793. Downdropped and rotated blocks of Eocene forearc may form a sub-basement beneath these flows in the central forearc basin; mid-Eocene basement was recovered at Sites 782 and 786 on the outer-arc high during Leg 125. Basement at Site 792 was defined using the vertical seismic profile (VSP) and logging data. Deep reflectors observed on the vertical seismic profile may originate in the Eocene sub-basement. Thick sequences of coarse-grained volcaniclastic and hemipelagic sediment fill the 70to 140-km-wide forearc sedimentary basin. Unrecovered (early Oligocene) strata beneath an unconformity, imaged by the multichannel seismic (MCS) line passing over Site 792, fill the deepest grabens of the central forearc and constitute Unit 4. The rapid deposition of volcaniclastics (Unit 3) during a dominant eruptive phase spanning much of the Oligocene, together with erosion of the basement highs bounding the basin, contributed to rapid subsidence and infilling. An inspection of cored materials from Unit 3 and logging data from Sites 792 and 793 reveals microfaults and other structural evidence for extension; on a much larger scale, MCS data show large normal faults near the frontal-arc high and outer-arc high that downfault the sediment section towards the central basin. Much of the largely pelagic or hemipelagic early Miocene section (Unit 2) has been removed by submarine valley formation and erosion, as at Sites 787 and 792. Middle Miocene to Holocene volcaniclastics and hemipelagics (Unit 1) top the forearc sedimentary section.

The post-middle Miocene evolution of sedimentary patterns in the eastern equatorial Pacific Ocean has been deduced from a compilation and synthesis of CaCO 3 , opal, and nannofossil assemblage data from 11 sites drilled during Leg 138.Improvements in stratigraphic correlation and time scale development enabled the construction of lithostratigraphic and chronostratigraphic frameworks of exceptional quality.These frameworks, and the high sedimentation rates (often exceeding 4 cm/k.y.) provided a detailed and synoptic paleoceanographic view of a large and highly productive region.The three highlights that emerge are: (1) a middle late Miocene "carbonate crash" (Lyle et al., this volume); (2) a late Miocene-early Pliocene "biogenic bloom"; and (3) an early Pliocene "opal shift".During the carbonate crash, an interval of dissolution extending from -11.2 to 7.5 Ma, CaCO 3 accumulation rates declined to near zero over much of the eastern equatorial Pacific, whereas opal accumulation rates remained substantially unchanged.The crash nadir, near 9.5 Ma, was marked by a brief shoaling of the regional carbonate compensation depth by more than 1400 m.The carbonate crash has been correlated over the entire tropical Pacific Ocean, and has been attributed to tectonically-induced changes in abyssal flow through the Panamanian seaway.The biogenic bloom extended from 6.7 to 4.5 Ma, and was characterized by an overall increase in biogenic accumulation and by a steepening of the latitudinal accumulation gradient toward the equator.The bloom has been observed over a large portion of the global ocean and has been linked to increased productivity.The final highlight, is a distinct and permanent shift in the locus of maximum opal mass accumulation rate at 4.4 Ma.This shift was temporally, and perhaps causally, linked to the final closure of the Panamanian seaway.Before 4.4 Ma, opal accumulation was greatest in the eastern equatorial Pacific Basin (near 0°N, 107°W).Since then, the highest opal fluxes in the equatorial Pacific have occurred in the Galapagos region (near 3°S, 92°W).

In the eastern and central Pacific Ocean the most profound change in Neogene calcium carbonate deposition occurred at the late/middle Miocene boundary (about 10 Ma), when carbonate mass accumulation rates (MARs) abruptly dropped.East of the East Pacific Rise (EPR), carbonate deposition essentially ceased.The carbonate compensation depth (CCD) in the Guatemala Basin, for example, rose by 800 m in less than 0.5 Ma.Even the rise crests suffered carbonate losses-Site 846, at the time less than 300 meters deeper than the EPR axis, experienced intervals between 10 and 9 Ma where no carbonate at all was buried.By about 8 Ma carbonate deposition resumed and was concentrated along an equatorial band, suggestive of high surface water carbonate production.East of the EPR, however, CCDs remained shallow since 10 Ma.This event which we have termed the late Miocene carbonate crash marks a fundamental paleoceanographic change that occurred in the eastern Pacific Ocean.Here, we document the changing pattern of carbonate deposition from 13 Ma to 5 Ma by using maps of carbonate MAR reconstructed from ODP Leg 138 and DSDP data.Comparisons to modern Oceanographic conditions demonstrate that the late Miocene carbonate crash could not have been caused by an abrupt increase in productivity at 10 Ma or by loss of C org from continental shelves.Instead it was probably caused by a relatively small reduction in deep-water exchange between the Atlantic and Pacific Oceans through the Panama Gateway prior to the emergence of the isthmus.A small restriction of deep-water exchange through this gateway is sufficient to radically change carbonate MARs in the eastern Pacific.

We calculate equations relating three different log-derived calcium carbonate estimates to laboratory measurements. Results indicate good correlations between the log and laboratory data sets, supporting the use of log data to derive carbonate stratigraphies. The best log estimate of laboratory values was generated from normalized yields of calcium, a method that can be completed on board ship. This method has the added advantage of providing the opportunity to guide shipboard sampling of the cores. Limitations of log methods result from potential depth mismatches, differences in the volumes measured, and the fact that logging tools and laboratory equipment are measuring different components of calcium carbonate (laboratory measurements are acid-soluble carbonate; log measurements are total calcium). Another limitation of using log data to estimate calcium carbonate is that log measurements alone cannot predict carbonate values directly. Some laboratory data are necessary to develop the regression equations that relate log data to CaCO3.

Correlation of the logs from the Izu-Bonin forearc sedimentary sections at Sites 787, 792, and 793 with the core data from Holes 787A-787B, 792A-792E, and 793A-793B allows the development of a more detailed lithostratigraphic model for those sites, and a more precise correlation of lithologic boundaries to basin-wide seismic reflections.Early Oligocene arc volcanics form the basement strata (Unit 5) sampled at Sites 792 and 793.Downdropped and rotated blocks of Eocene forearc may form a sub-basement beneath these flows in the central forearc basin; mid-Eocene basement was recovered at Sites 782 and 786 on the outer-arc high during Leg 125.Basement at Site 792 was defined using the vertical seismic profile (VSP) and logging data.Deep reflectors observed on the vertical seismic profile may originate in the Eocene sub-basement.Thick sequences of coarse-grained volcaniclastic and hemipelagic sediment fill the 70-to 140-km-wide forearc sedimentary basin.Unrecovered (early Oligocene) strata beneath an unconformity, imaged by the multichannel seismic (MCS) line passing over Site 792, fill the deepest grabens of the central forearc and constitute Unit 4. The rapid deposition of volcaniclastics (Unit 3) during a dominant eruptive phase spanning much of the Oligocene, together with erosion of the basement highs bounding the basin, contributed to rapid subsidence and infilling.An inspection of cored materials from Unit 3 and logging data from Sites 792 and 793 reveals microfaults and other structural evidence for extension; on a much larger scale, MCS data show large normal faults near the frontal-arc high and outer-arc high that downfault the sediment section towards the central basin.Much of the largely pelagic or hemipelagic early Miocene section (Unit 2) has been removed by submarine valley formation and erosion, as at Sites 787 and 792.Middle Miocene to Holocene volcaniclastics and hemipelagics (Unit 1) top the forearc sedimentary section.

We examine the physical properties of volcaniclastic sediments in the forearc and backarc of the Izu-Bonin arc region.Based on our analyses of these and other deposits in the area, we conclude that, with the possible exception of pumice-rich material, unlithified volcaniclastics behave much like detrital deep-sea sediments.In contrast, lithified volcaniclastic sediments display unique physical properties, such as higher electrical resistivity and velocity than expected from porosity values.The primary cause of these phenomena is a lack of interconnectedness of the pore spaces and cementation of the volcaniclastic particles.

Sediment dry-bulk density values are essential components of mass accumulation rate calculations. This manuscript presents three equations to calculate dry-bulk density from laboratory measurements of physical properties that have been corrected for the salt content of the pore fluid. In addition, two equations for use with values not corrected for salt content are included. Derivations of the equations from first principles are presented. The second part of the manuscript briefly examines laboratory measurements of the various properties used in the dry-bulk density equations. A discussion of the problems inherent in the density measurements and recommendations are included. This work represents the first comprehensive compilation of equations of dry-bulk density and should prove useful to all scientists who investigate accumulation rates.