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Holocene sedimentation in the southern Gulf of California and its climatic implications

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Holocene sedimentation in the southern Gulf of California and its climatic implications

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Content HOLOCENE SEDIMENTATION IN THE SOUTHERN GULF OF CALIFORNIA AND ITS CLIMATIC IMPLICATIONS. by Oscar Efraln Gonzalez-Yajimovich A Dissertation Presented to the FACULTY OF THE GRADUATE SCHOOL UNIVERSITY OF SOUTHERN CALIFORNIA In Partial Fulfillment of the Requirements of the Degree DOCTOR OF PHILOSOPHY (GEOLOGICAL SCIENCES) August 2004 Copyright 2004 Oscar Efrain Gonzalez-Yaj imovich Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. UMI Number: 3145204 INFORMATION TO USERS The quality of this reproduction is dependent upon the quality of the copy submitted. Broken or indistinct print, colored or poor quality illustrations and photographs, print bleed-through, substandard margins, and improper alignment can adversely affect reproduction. In the unlikely event that the author did not send a complete manuscript and there are missing pages, these will be noted. Also, if unauthorized copyright material had to be removed, a note will indicate the deletion. ® UMI UMI Microform 3145204 Copyright 2004 by ProQuest Information and Learning Company. All rights reserved. This microform edition is protected against unauthorized copying under Title 17, United States Code. ProQuest Information and Learning Company 300 North Zeeb Road P.O. Box 1346 Ann Arbor, Ml 48106-1346 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. DEDICATION To Jennifer, Oscar and Erica Many times I come home late after a long day and fin d you still studying or doing chores, you are always an example to follow. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Acknowledgments My appreciation to my advisors Robert Douglas and Donn Gorsline, their character and knowledge are the definition of a professor. Donn opened the doors and paved my way to USC. He was always attentive to my work and ready to help. Bob’s advice and patience were essential for this investigation. The conversations with Bob on the 110 commute are one of the highlights of my time in southern California and I will really miss them. The Douglas’ always made me feel like part of the family, their kind hospitality is dearly appreciated. I owe many thanks to the members of my dissertation committee; Frank Corsetti’s support and advice started when I met him my first day at USC and has continued since. Dr. Enrique Nava Sanchez was always enthusiastic about my research and provided invaluable advice and help with fieldwork and logistics in La Paz. Professor Jiin-Jen Lee’s advice and corrections to the manuscript are much appreciated. Professor Lowell Stott welcomed me to his lab to perform carbon and nitrogen analyses. His help along with Miguel Rincon’s assistance are greatly appreciated. Dr. Walter Daessle Heuser allowed me to use the grain size and elemental analyzers at UABC, and Arturo Siqueiros trained me in the use of the instruments. Alberto Sanchez’s help with the biogenic opal analysis was invaluable. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. My gratitude to all the participants and crew of the R/V New Horizon. The time at sea during the CALMEX cruise aboard the was not only productive but also enjoyable. Sediment trap samples and data were provided by Dr. Norman Silverberg and Fernando Aguirre (CICIMAR) and were essential for this investigation. I was lucky to have been invited to participate in one of the recovery/set up cruises and value the learning experience. Dr. William Berelson kindly provided 2 1 0 Pb Age determinations for the CALMEX cores. The United States Geological Survey at the Livermore National Laboratory and at the National Center in Reston, did the 1 4 C age determinations. Several people were always willing to help with advice and/or training in the different instruments used in this research. Many thanks to Professor Douglas Hammond, Dr. John Barron (USGS), Dr. Hongchun Li, Francisca Staines-Urias, Dr. Teresa de Diego Forbis, Tran Hyun, Maria Prokopenko, Professor Richard Berry (UCSD), and Dr. Janette Murillo (CICIMAR), Erica Gonzalez Davis’ help with running the coulometer effectively reduced the sample processing time in half. Marlene Pina Arce (UABCS) was a big help in setting up and tending to the dust traps. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. V My gratitude to the faculty of the Geology department at UABC for all their support and encouragement. Special thanks to Luis Cupul Magana who was my liaison in Ensenada during my stay in Los Angeles. Thanks Dr. Roberto Millan Nunez, director of the School of Oceanography at UABC for facilitating my coming to USC. My stay at USC was funded through a fellowship from the Program for Faculty Improvement UABC/SEP (PROMEP) and a Last Year Dissertation Fellowship from the USC Department of Earth Sciences. Funding for this research was provided by grants from the National Science Foundation International Programs (US-Mexico) INT 0304933 to Robert G. Douglas and Donn S. Gorsline and (Ocean Sciences) OCE 0002250 to Lowell D. Stott, Robert G. Douglas and William Berelson. The Consejo Nacional de Ciencia y Tecnologla (Paleoceanografia del Holoceno en el Golfo de California y el Borde Continental Califomiano, Mexico) N° 365 to Jorge Ledesma-Yazquez, the Graduate Student Research Fund of the Earth Sciences Department at USC and Fox Studios Baja. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. vi TABLE OF CONTENTS Page DEDICATION ii ACKNOWLEDGEMENTS iii LIST OF TABLES ix LIST OF FIGURES x ABSTRACT xviii 1 INTRODUCTION 1 1.1 Objectives 1 1.2 Introductory Background 2 2 GEOLOGIC SETTING 9 2.1 Study Area 9 2.2 Tectonics 10 2.2.1 Subduction Regimen 10 2.2.2 Extension 11 2.2.3 Continental Rifting 14 3 CLIMATE AND OCEANOGRAPHY 17 3.1 Climate 17 3.2 Water masses and Circulation 18 3.3 Oxygen Minimum Zone 23 3.4 Climatic Indices: ENSO, PDO and others 24 4 METHODOLOGY 28 4.1 Core Collection And Curation 28 4.2 Age-Depth Models 30 4.3 Grain Size Analysis 35 4.4 Density Profiles (Grape) 36 4.5 Mass Accumulation Rates 37 4.6 Sediment Components 38 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 4.6.1 Biogenic Opal Content V 38 4.6.2 Total Carbon Content 39 4.6.3 Total Organic Carbon Content 39 4.6.4 Carbonate content 39 4.7 Eolian Sediment Traps 40 4.8 Sediment Trap 42 4.9 X-Ray Diffraction 42 4.10 Spectral Analysis 45 5 ALFONSO AND EASTERN PESCADERO BASINS SEDIMENTARY RECORD 46 5.1 Review and Previous Work. 46 5.2 Results 53 5.2.1 Age-Depth Models 53 5.2.2 Grain Size Analysis 61 5.2.3 Density, Porosity and Mass Accumulation Rates 70 5.2.4 Terrigenous Sediment for all cores 77 5.2.5 Biogenic Opal Content 100 5.2.6 Total Carbon Content 113 5.2.7 Organic Carbon Content 118 5.2.8 Carbonate Content 118 5.2.9 Variability Cycles Observed 137 6 CONCLUSIONS 149 7 REFERENCES 152 8 APPENDICES 163 A. Sedimentation Rates from X-Ray Grayscale in all cores. 164 B. Grain Size Parameters for all cores (pm). 169 C. Porosity (POR), Dry Bulk Density (DBD) and Total Mass Accumulation Rates (TMAR) in all cores. 179 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. viii D. Summary of dust trap recovery data and flux estimates. 188 E. Percentage and MAR of terrigenous Sediment in all cores. 189 F. Percentage and MAR of Biogenic Opal in all cores. 194 G. Percentage and MAR of Total Carbon in all cores. 198 H. Percentage and MAR of Organic Carbon in all cores. 202 I. Percentage and MAR of CaC03 in all cores. 207 J. Summary of cycles obtained with MTM Spectral Analysis in all 211 cores. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. ix Table 1 Table 2 Table 3 Table 4 Table 5 LIST OF TABLES Summary of characteristic TS values for the water masses in the Gulf of California. From Torres-Orozco, (1993). Core locations, lengths and depths. Table includes CALMEX and BAP cores used in this study and those used by Bemal-Franco (2001). Results of radiocarbon dating for CALMEX cores used in this investigation. Calibration was done using the CALIB 4.4.1 database of Stuvier and Reimer, (1993a). Reservoir age used was 574±18 based on Frantz et al., 2000. Last column shows dates standardized to 2000 AD (+50years). Comparison of results of the grain size analysis following Rea and Hovan (1995) method to their source end- members. Sediments from Alfonso Basin are consistent with a hemipelagic source. Summary of MTM spectra for all cores and records. Page 22 29 58 87 137 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. X Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 LIST OF FIGURES Page Gulf of California showing the location of cores, sediment 8 trap and dust traps used in this study. A simplified bathymetry is included for Alfonso and Pescadero Basins. Baja California peninsula and adjacent mainland North 13 America, showing the southern Basin Range Province and the Gulf Extensional Province. From Stock and Hodges, (1989). Tectono-sedimentary model of three-dimensional structure 15 and sedimentary environments in early stages of syn-rift evolution of rift basin. From Leeder (1995). Seasonal Surface wind climatology for the December- 19 January (a), March-April-May (b), June-July-August (c) and September-October-November (d) periods. From Pares- Sierra et al. (2003). Gulf of California’s Mean Air Temperature (C°) for the 20 months of January (a) and July (b), and Mean Annual Rainfall (c), and Mean Percentage of Summer Rain, May to October (d). From Roden (1964). Temperature and salinity diagram for CTD soundings at the 21 entrance to the Gulf of California showing water masses present. ASE = Tropical Surface Water, AGC = Gulf of California Water, ACC = California Current Water, AsSt = Subtropical Subsurface Water, AIP = Pacific Intermediate Water and APP = Pacific Deep Water. From Castro et al., (2000). (top) Normalized winter mean time histories of Pacific 27 climate indices. Dotted vertical lines are drawn to mark the Pacific Interdecadal Oscillation (PDO) polarity reversal times in 1925, 1947, and 1977. Positive value bars are filled with black, negative with gray shading, (bottom) SST and SLP (contoured) regressed upon the PDO for the period of 1900-1992. From Mantua, et al. (1997). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Figure 8 Figure 9 Figure 10 Figure 11 Figure 12 Figure 13 Figure 14 Figure 15 Figure 16 Figure 17 xi Example of an X-radiograph along with digital grayscale 34 and dry bulk density profile, section corresponds to the 60- 86 cm portion of core NH01-15GC3. Dust trap used, (top) The design developed by the U.S. 41 Geological Survey consists of an angel food cake pan mounted on a steel fence post, (bottom) Setting the trap at El Coyote location. Schematic diagram showing Alfonso Basin’s sediment trap 43 mooring. A Technicap Sediment Trap Model PPS-3/3 (1/8 m" aperture) was used. From Silverberg et al. (2003). Technicap PPS-3/3 sediment trap on deck on the BO Ulloa 44 after recovery. Photo courtesy of Fernando Aguirre Bahena. Bathymetric chart of La Paz Bay and Morphological section 47 showing the structure and position of Alfonso basin as well as the general sedimentation patterns. Contours every 50 meters. After Nava Sanchez (1997). X-Radiographs of sediments from the Gulf of California. A) 52 Guaymas-type laminations. Sharp contrasting lamina characterizes this sediment. B) Alfonso-type laminations characterized by wavy and sometimes discontinuous boundaries. Age model for Alfonso Basin (station BAP96-CP) based on 55 Radiocarbon calibrated and excess 2 1 0 Pb data. Data from Douglas et al. (2002b). Age model for Alfonso Basin (BAP94-CB) station based on 56 correlation with core BAP96-CP. Age model for Alfonso Basin (CALMEX NH01-15) station 60 based on radiocarbon calibrated and excess 2 1 0 Pb data. Age model for East Pescadero Basin (CALMEX NH01-26) 62 station based on radiocarbon calibrated data. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Figure 18 Figure 19 Figure 20 Figure 21 Figure 22 Figure 23 Figure 24 Figure 25 Figure 26 Figure 27 xii Median grain size downcore for CALMEX NHQ1-15 63 composite core (GC3 and MCI), Alfonso Basin, Gulf of California. An 81cm turbidite has been removed from the record. See text for explanation. Mean grain size downcore for CALMEX NHO1-15 64 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. An 81cm turbidite has been removed from the record. See text for explanation. Grain Size Standard Deviation downcore for CALMEX 65 NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. An 81cm turbidite has been removed from the record. See text for explanation. Median grain size downcore plot for CALMEX NH01-26 67 composite core (GC1 and M CI), East Pescadero Basin, Gulf of California. Mean grain size downcore plot for CALMEX NHO 1-26 68 composite core (GC1 and M CI), East Pescadero Basin, Gulf of California. Intervals for the Holocene are included. Grain size standard deviation downcore plot for CALMEX 69 NHO 1-26 composite core (GC1 and M CI), East Pescadero Basin, Gulf of California. Dry bulk density and porosity in CALMEX NHO 1-15 71 composite core (GC3 and M CI), Alfonso Basin, Gulf of California Total mass Accumulation Rates for NH01-15 composite 72 core (GC3 and M CI), Alfonso Basin, Gulf of California. Dry Bulk Density and Porosity in CALMEX NHO 1-26 73 composite core (GC1 and M CI), Eastern Pescadero Basin, Gulf of California. Total mass accumulation rates for NHO 1-26 composite core 75 (GC1 and M CI), eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Figure 28 Figure 29 Figure 30 Figure 31 Figure 32 Figure 33 Figure 34 Figure 35 Figure 36 Figure 37 Figure 38 Figure 39 xiii Ten point running average of total mass accumulation rates 78 for cores NH01-15 and NH01-26. X-ray diffractogram of sample NHO 1-GC3-21. Non-mineral 80 components removed X-ray diffractogram of sample NH01-GC3-184. Non- 81 Mineral components removed. X-ray diffractogram of sample NH01-15GC3-241. Non- 82 mineral components removed. X-ray diffractogram of samples from the San Juan and El 83 Coyote fans. A factor of 100 was added to El Coyote for graphic purposes. X-ray diffractogram of Isla Ballena Dust Trap. 84 Examples of results from Grain Size analysis for samples in 86 where the non-mineral components where selectively removed as per Rea and Hovan (1995) proposed methodology. Gulf of California showing the location of ephemeral 88 streams around the La Paz bay and the main rivers on the eastern margin. Terrigenous content weight % for CALMEX NHO 1-15 90 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Terrigenous mass Accumulation Rates for CALMEX NHO 1- 91 15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Terrigenous mass accumulation rates for core BAP96-CP, 92 Alfonso Basin, Gulf of California. Terrigenous sediment weight % in CALMEX NHO 1-26 94 composite core (GC1 and M CI) for Eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Figure 40 Figure 41 Figure 42 Figure 43 Figure 44 Figure 45 Figure 46 Figure 47 Figure 48 Figure 49 x i v Terrigenous Sediment mass accumulation rates in CALMEX 95 NHO 1-26 composite core (GC1 and M CI) for Eastern Pescadero Basin, Gulf of California. Terrigenous MAR records from the southern Gulf of 96 California illustrating the climatic periods during the Holocene. The center column indicates the inferred average position of the Intertropical convergence Zone. The right column lists the general characteristics of the period. Mass accumulation rates in mg/cm2 /year. Mass accumulation rates of the terrigenous component in 98 NH01-15 record plotted against May to October integrated insolation for latitude 24°N. Mass accumulation rates of the terrigenous component in 99 NH01-26 record plotted against May to October integrated insolation for latitude 24°N. Biogenic opal content weight % core BAP96-CP, Alfonso 101 Basin, Gulf of California. Biogenic opal mass accumulation rates for core BAP96-CP, 102 Alfonso Basin, Gulf of California. Biogenic opal content weight % for CALMEX NHO 1-15 103 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Biogenic opal mass accumulation rates for CALMEX 105 NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Biogenic opal content weight % in Calmex NHO 1-26 106 composite core (GC1 and M CI) for Eastern Pescadero Basin, Gulf of California. Biogenic opal content mass accumulation rates in CALMEX 107 NHO 1-26 composite core (GC1 and M CI) for Eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. XV Figure 50 Figure 51 Figure 52 Figure 53 Figure 54 Figure 55 Figure 56 Figure 57 Figure 58 Figure 59 Figure 60 Biogenic opal MAR records from the southern Gulf of 111 California illustrating the climatic periods during the Holocene. The center column indicates the inferred average position of the Intertropical convergence Zone. The right column lists the general characteristics of the period. Mass accumulation rates in mg/cm2 /year. Total carbon content for NH01-15 composite core (GC3 and 114 M CI), Alfonso Basin, Gulf of California. Total carbon mass accumulation rates for NHO 1-15 115 composite core (GC3 and MCI), Alfonso Basin, Gulf of California. Total carbon content weight % in CALMEX NHO 1-26 116 composite core (GC1 and M CI) for Eastern Pescadero Basin, Gulf of California. Total carbon mass accumulation rates in CALMEX NHO 1- 117 26 composite core (GC1 and MCI), Eastern Pescadero Basin, Gulf of California. Organic carbon content weight % for core BAP96-CP, 119 Alfonso Basin, Gulf of California. Organic carbon mass accumulation rates for core BAP96- 120 CP, Alfonso Basin, Gulf of California. Organic carbon content weight % for CALMEX NHO 1-15 121 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Organic carbon mass accumulation rates for CALMEX 122 NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Total organic carbon content weight % in CALMEX NH01- 123 26 composite core (GC1 and M CI), Eastern Pescadero Basin, Gulf of California. Total organic carbon mass accumulation rates in CALMEX 124 NHO 1-26 composite core (GC1 and M CI), Eastern Pescadero Basin, Gulf o f California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. xvi Figure 61 Figure 62 Figure 63 Figure 64 Figure 65 Figure 66 Figure 67 Figure 68 Figure 69 Figure 70 Figure 71 Figure 72 Scanning electron microscope (SEM) image of a light 125 colored lamina, core CP 164 cm. Composition is mainly coccolithophoridae debris with clay and diatom fragments. Carbonate content weight % in core BAP96-CP, Alfonso 127 Basin, Gulf of California. Carbonate mass accumulation rates for core BAP96-CP, 128 Alfonso Basin, Gulf of California. Carbonate content weight % in BAP96-CB core, Alfonso 129 Basin, Gulf of California. Top 5 cm missing. Carbonate content for NH01-15 composite core (GC3 and 130 M CI), Alfonso Basin, Gulf of California. Carbonate mass accumulation rates for NHO 1-15 composite 131 core (GC3 and M CI), Alfonso Basin, Gulf of California. Carbonate content weight % in CALMEX NHO 1 -26 133 composite core (GC1 and M CI) for Eastern Pescadero Basin, Gulf of California. Carbonate content mass accumulation rates in CALMEX 134 NHO 1-26 composite core (GC1 and M CI) for Eastern Pescadero Basin, Gulf of California. Power spectra calculated for the carbonate record in Alfonso 138 Basin. Top, core CB; bottom, core CP. Frequency in cycles/year. Power spectra calculated for the carbonate record in Alfonso 139 and eastern Pescadero Basins. Top, core 15; bottom, core 26. Frequency in cycles/year. Power spectra calculated for the organic carbon record in 140 Alfonso and eastern Pescadero Basins. Top, core 15; bottom, core 26. Frequency in cycles/year. Power spectra calculated for the biogenic opal record in 141 Alfonso and eastern Pescadero Basins. Top, core 15; bottom, core 26. Frequency in cycles/year. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. x v i i Figure 73 Figure 74 Figure 75 Power spectra calculated for the terrigenous content record 142 in Alfonso and eastern Pescadero Basins. Top, core 15; bottom, core 26. Frequency in cycles/year. Power spectra calculated for grain size parameters in 143 Alfonso Basin. Frequency in cycles/year. Power spectra calculated for grain size parameters in eastern 144 Pescadero Basin. Frequency in cycles/year. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. x v iii ABSTRACT Alfonso Basin on the western side of the G ulf of California and Pescadero Basin on the center slope of the east side of the gulf are margin basins which have sills or shoreward slopes in the Oxygen Minimum Zone and preserve laminations whose physical and geochemical characteristics yield information on climatic and oceanographic changes. Here primary productivity and sedimentation can be considered as an imperfect proxy of climate. Cores were sampled at 1 cm intervals to produce a record of organic carbon, carbonate, opal and terrigenous content and contained laminated, hemipelagic mud, accumulating at 25-50 cm/kyr. Sediment cores from Alfonso Basin are organic carbon-rich (5-7%) with varying carbonate (1- 25%) and little opal (<4%) and span 7700 YBP. Sediment cores from Eastern Pescadero are also organic carbon-rich (2.5-4.3%) but contain less carbonate (0-6%) and more silica (8-21%) and record 9083 YBP. Major changes in sedimentation began at circa 7,200 YBP with major shifts occurring at 4,200 and 3,000 YBP and smaller changes at 1500, 950, and 400 YBP in both basins. A stepwise decrease in mass accumulation rates can be correlated to northern hemisphere summer insolation, and suggests stronger NW winds and decreasing rains. Biogenic records indicate a drop in productivity and terrigenous mud records a shift from wetter to dryer conditions. At 400 YBP a recovery suggests a return to wetter less windy conditions. Three general climatic periods are recognized; an early period (10,000- 7,200 YBP) with high productivity and variability resulting from strong northwesterly winds and upwelling; A middle period (7,200-4,200 YBP) a stable Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. period with steady decrease in productivity. And a late period (4,200 YBP to the present) with constant primary productivity suggested by opal fluxes, and with an increase in the carbonate-opal east-west asymmetry. Spectral analysis shows a 1-2 kyr climate rhythm in the Gulf and the data suggest that it is mediated by the migration of the Intertropical Convergence Zone (ITCZ) due to orbital precession. The records are marked by strong climate-ocean variability cycles with two modes: 210 years (throughout the record) and 800 years (after 3000 YBP) that appear related to latitudinal shifts of the ITCZ, produced by solar cycles. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 1. INTRODUCTION 1.1 Objectives The central objective of this investigation is to understand the formation and preservation of the sedimentary record in Alfonso and eastern Pescadero Basins as a basis for interpreting the Holocene oceanographic and climatic processes operating in the Gulf of California, and particularly those that record multidecadal to millennial cycles. Most of the sedimentary records investigated in the Gulf of California are from Guaymas basin in the central region. An objective of this work is to contribute to the understanding of the Gulf by generating a Holocene sedimentary record for the southern portion, an area under the influence of both the Mexican monsoon and the open Pacific Ocean. Previous research has revealed an east-west asymmetry in the sedimentary record for the southern Gulf; an objective of this investigation is to determine what oceanographic/climatic processes control sedimentation in two opposing basins in the southern Gulf. Previous studies have shown that the sediments in Alfonso Basin contain high silt-clay content but it is unclear what proportion of the fine-grained material is of eolian versus fluvial origin. An objective of this investigation is to determine the source of the terrigenous component in the sediment laminations. Preliminary work based on excess 2 1 0 Pb profiles suggests a large variation in sedimentation rates between the shelf and basin floor, but these rates are at present poorly constrained. Preliminary work also suggests variations within the basin, which represent variations in productivity and/or paleoceanographic conditions. A Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. basic aspect of the investigation is to develop depth-age models, which could be used to calculate sedimentation and mass accumulation rates o f sediments in the basins. Another goal is to reconstruct biogenic input and paleoproductivity from measurements of total organic carbon, carbonate and biogenic opal, and to answer the important question of how the present flux rates of the major biogenic components from the water column compare to basin input in the past. 1.2. Introductory Background Growing evidence from deep-sea sediments, ice cores and pollen reveal that Holocene climates are unstable and punctuated by changes that are part of a 1500 ± 500 yr quasi-periodic climate rhythm. This rhythm is independent of the glacial- interglacial cycles, and was first detected in the North Atlantic (Bond et al., 1997; McManus et al., 1999; Oppo et al., 1998; Raymo et al., 1998), and recently elsewhere (Bond et al., 2001; Campbell et al., 1998; DeMenocal et al., 2000; Viau et al., 2002), but observed as early as the 1800’s in climatic histories (Blytt-Semander zonation) interpreted from peat bogs in northern Europe (Flint, 1971). The variations found in different proxies are large-scale in nature and confirm that Holocene and late glacial climate variations of millennial scale were abrupt transitions between climatic regimens as the atmosphere-ocean system reorganized in response to forcing (Viau et al., 2002). Recent evidence points to a potential solar forcing associated with ocean-atmosphere feedbacks (Bond et al., 2001). Much of the paleoclimatic research effort in the past decade has focused on the investigation of the skeletal remains of organic productivity preserved in the Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. sediments on the bottom of the ocean and detritals from physical processes: biogenic and terrigenous sediments. Biogenic sediments are produced in surface waters and exported to the seafloor. Primary productivity is climatically driven by atmospheric circulation, which creates conditions of upwelling and oceanic divergence that advect nutrient- rich deep waters to the surface. In the Gulf of California, the “Mexican Monsoon” (Douglas et al., 1993) drives primary productivity by generating winds that blow from north to south from the late fall to early spring, creating strong upwelling and a thick mixed layer. These conditions lead to eutrophy and high primary productivity over most of the central and northern Gulf (Alvarez-Borrego and Lara-Lara, 1991; Thunell, 1996), with a corresponding high flux of skeletal material to the bottom. Opal silica dominates biogenic sedimentation in the northern Gulf, with diatoms being the main constituent. Lesser amounts of carbonate debris is produced. Bacterial decomposition of the high organic carbon input leads to carbon dioxide, carbonic acid and dissolution of the carbonate component (Berger, 1973). Despite the high production rates, dissolution rapidly removes carbonate from the sediment. Based on sediment trap data, a 70% to 80% fraction o f export carbonate is remineralized either in route or shortly after reaching the sea floor (Calvert, 1966; Pride et al., 1999). In the summer and early part of the spring the winds weaken and the pattern reverses creating a well-stratified ocean and oligotrophic conditions more conducive to carbonate sedimentation and preservation (Douglas et al., 2002b). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Towards the mouth of the Gulf primary productivity is lower and both silica and carbonate are exported to the bottom. Terrigenous sediments are derived from the continents and transported to receiving basins by two major transport mechanisms: eolian and fluvial. During the winter-spring period when strong northerly winds prevail, eolian dust is an important source o f fine terrigenous sediment. In many ocean regions the major constituents of marine aerosols is soil material derived from arid desert regions on the continents (Prospero, 1981; Rea, 1994). Determining the basic characteristics of these sediments and comparing them to those preserved in the ocean record is important to modeling paleoceanographic conditions and determining source regions. This, in turn can also be useful in determining climate conditions at the time o f deposition and evaluating the effects of modem land use. In most desert areas, dust comes from in situ weathering of bedrock (Goudie, 1978), as well as from alluvial fans and deposits on dry flood plains. Two other important sources in arid and semiarid regions are widespread agricultural fields that expose fine-grained particles for deflation, especially during periods of drought and when regions are stripped of their natural vegetation by urban development, construction, and by the use of off-road vehicles (Nakata et al., 1981; Pewe, 1981). In the central Gulf o f California, Baumgartner et al. (1991b), found that the major constituent of the dark layer in 20th century varves was fine-grained material transported by wind. The Bay of La Paz is surrounded by arid land and with a wind regime that blows from the northeast during the winter season and from the southwest during the summer. These southwesterly winds could Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 5 be responsible for the high content of terrigenous fine-grained sediments found in cores recovered in this region. Summer tropical storms and El Nino-Southern Oscillation events account for most of the rainfall in the Gulf and fluvial sediments accumulate in fan deltas in the western margin and in river deltas on the gently sloping eastern margin (Nava- Sanchez, 1997). The finer components of these fluvial sediments are moved to the slope and deep basins were they are deposited as turbidites and/or hemipelagic sediments. On the Eastern margin, the runoffs from the Chihuahua and Durango Sierras through the coastal state of Sinaloa provide the bulk o f terrigenous sediments to the margin and eventually to sedimentary basins in the southern Gulf of California. The mean annual runoff o f this state is 15,169 million cubic meters, the main rivers and in parenthesis their corresponding mean annual runoff in millions of cubic meters are: the Fuerte (4838), Flumaya (1715), Sinaloa (1608), San Lorenzo (1572), Baluarte (1518), Piaxtla (1357) and Presidio (1082) (Gobiemo del Estado de Sinaloa, 2004). These compare to the Colorado (17,000) before the completion of Hoover Dam in 1935 (Rodriguez et al. 2001), which dominates the northern Gulf. On the Western margin the main runoffs that provide the terrigenous sediments that eventually end up in the slope basins are the El Coyote and San Juan arroyos (Nava- Sanchez, 1997) In the Gulf of California lithogenic and biogenic components are deposited as laminated sediments with couplets of light and dark-colored lamina, thin flood layers and turbidites. Light-colored lamina are mainly biogenic, composed of coccoliths Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 6 and diatoms and the dark lamina are composed of coarse silt and organic debris (Calvert, 1966; Donegan and Schrader, 1982). Several researchers have studied the nature and origin of the laminated sediments in the Gulf of California proposing different mechanisms for the two types of lamina. Calvert (1966) suggested continuous deposition of diatoms with pulses of high lithic detritus during the summer rainy season from river runoff. Baumgartner et al. (1991b) proposed seasonally varying flux of both diatoms and detritus. Sancetta (1995) identified three types of lamina: 1) Lithogenic lamina composed mainly of clays and silt with minor diatomaceous material. These lamina represent the wet season. However, the average thickness does not show significant variations during 20th century records, that could imply that the main sediment source is different than the river discharges; 2) Mixed flora diatomaceous lamina that represent early winter. At this time a wind transition occurs in the area and the water column stratification breaks down (thermocline collapse). The abundances of faecal pellets indicate high zooplankton abundances. 3) Near monospecific flora lamina (Chaetoceros, sp. Resting spores) that represent spring coastal upwelling blooms. Pike and Kemp (1997), using scanning electron microscopy were able to resolve up to five depositional events per year. Clay and silt and abundant diatom spores typify a summer to early autumn layer. An early winter lamina is composed of a “dump flora”, which includes diatom mats. A diatom flora follows these during the main winter windy season, and when upwelling dies down the floras become nearly monospecific. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 7 Several factors contribute to the variability observed in the laminations, including a bathymetry of the receiving basin that favors accumulation and low concentration of oxygen to inhibit benthic bioturbators. The Gulf of California is a unique region in which we find several basins that fulfill these requirements, among them Alfonso Basin, a small suboxic basin inside the Bay of La Paz, Baja California Sur, and Pescadero Basin located in deeper waters in the central region o f the gulfs entrance (Figure 1). The locations of the southern Gulf basins allow for the deposition of sediments of continental and marine origin. Because of its high productivity (Alvarez Borrego, 1983; Alvarez-Borrego and Lara-Lara, 1991; Thunell, 1996) the Gulf of California generates a lot o f biogenic sediment, and given its topographic configuration it also captures terrigenous sediments generated from the regions of Sonora and Sinaloa and from the Baja California peninsula. Productivity and terrigenous sedimentation are driven by climate in the Gulf region in a monsoon-like system that generates alternating dominance between the two main sediment types. Alfonso and Pescadero Basins are located near the junction of the Gulf and the open Pacific Ocean recording seasonal variation in the Gulf and the larger scale climate conditions of the subtropical Pacific (Douglas et al., 2002b). This and the fact that the Gulf has a very distinct oxygen minimum zone, accounts for an excellent preservation of the primary sedimentary record (Bernal Franco, 2001; Calvert, 1966). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 8 S e d im e n t t r a p l o c a t io n Dust t r a p LOCATIONS Gr a v it y a n d M u lti Core l o c a t io n s A lfo nso B a s in La Paz •'Basin B o c a G r a n d e P escadero / B a s in Sinaloa 2000 500 1000 1000 .a Paz 8AJA i Ca lifo r n ia Sur / 2000 Figure 1. Gulf of California showing the location of cores, sediment trap and dust traps used in this study. A simplified bathymetry is included for Alfonso and Pescadero Basins. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 2. G EO LOG IC SETTING 2.1 Study Area The study area is located in the southwestern margin of the Gulf of California and the central portion of the gulfs entrance. Cores from two basins were recovered and used in this investigation: Alfonso and eastern Pescadero Basins. Alfonso Basin centered at 24°40’ N and 110° 38’ W, is a small, closed depression (maximum depth 400 m) with an effective depth of about 320 m (deepest sill) and a width of 22.2 km and length of 25km (Nava-Sanchez et al., 2001) (Figure 1). Deep water entering the basin is drawn from low-oxygen intermediate waters and, below 200 m the basin is suboxic to anoxic. Alfonso Basin has been classified as a slope basin produced by extensional tectonics in a borderland type margin setting (Nava-Sanchez et al., 2001). Pescadero Basin is located at the entrance of the Gulf centered at 24°15’ N and 109° 00’ W, it has depths that reach a maximum of more than 2,500 m and it has an elongated form with a breadth of about 200 km. This position and depth allows for free exchange between waters of the Pacific and the Gulf (Castro et al., 2000). Because of their location near the junction of the Gulf and the open Pacific Ocean, these sites are sensitive recorders of the monsoon-driven seasonal variations in the Gulf and the larger-scale climate circulation of the subtropical Pacific Ocean (Douglas et al., 2002b). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 10 2.2 Tectonics The Baja California peninsula and adjacent Gulf of California off the Mexican mainland evolved through three phases of development in Miocene to Recent times. The first is represented by a subduction regime active from 24 to about 12 Ma on the Pacific coast of Baja California during which the Farallon plate was being subducted under western Mexico (Hausback, 1984). The second is a major episode o f crustal extension related to the opening o f the proto-Gulf of California (10 to 3.5 Ma) a process distally related to Basin and Range tectonics in western North America (Karig and Jensky, 1972; Stock and Hodges, 1989). The final stage is the transtensional regime or the generation of crustal deformation in oblique zones of ocean spreading that consists of stepped transform faults. Here, the two elements of extension and strike-slip motion combined and are considered responsible for the present tectonic configuration in the Gulf of California (Mayer and Vincent, 1999; Zanchi, 1994) and the total transfer of Baja California to the Pacific Plate from the North American Plate. The major sedimentary basins evolved during the main extensional episode and the transtensional regime, and the sedimentary evolution of these basins is neither simple nor unique (Mayer and Vincent, 1999; Stock and Hodges, 1989; Zanchi, 1994). 2.2.1 Subduction Regimen As the Farallon plate was subducted beneath North America, during the early Tertiary, Baja California was a stable marine continental shelf receiving volcanic detritus from the active Sierra Madre Occidental volcanic arc in Western Mexico. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 11 Volcanic activity migrated westward and arrived along what is now eastern Baja California about 24 ma ago accompanied by uplift of the Baja California platform. Volcanism dominated the geological events o f the peninsula from about 24 ma to 12 ma. The focus for this volcanic activity lay along the eastern margin o f the present peninsula of Baja California. The volcanic and volcaniclastic materials that constitutes the Isidro and Comondu formations were shed to the west from the arc, first into a shallow marine shelf, then onto a network of volcanic and detrital non marine fans built across Baja California. These arc-related volcanic rocks range from andesitic flows and lahars to rhyolitic ash-flow tuffs. The abundance of rhyolitic volcanics generally decreases to the north from the Bay o f La Paz region (Nava- Sanchez, 1997; Hausback, 1984). Subduction ceased off Baja California by 12 ma ago (Hausback, 1984), closely followed by the extinction of the Comondu volcanic arc. Consumption of the Farallon plate resulted in the juxtaposition of the Pacific plate with Baja California along the Tosco-Abreoj os fault. Lack of depositional units above the Comondu volcanics indicates a separation of the peninsula from the easterly volcanic and sedimentary sources probably due to graben formation along the locus of a proto- Gulf of California (Hausback, 1984). 2.2.2 Extension The opening of the Gulf of California is often attributed to two sequential events: middle to late Miocene “proto-Gulf’ extension and Pliocene development of Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 12 the Pacific-North America plate boundary, from about 5.5 ma ago to the present (Stock and Hodges, 1989; Lyle and Ness, 1991). Originally, the proto-Gulf concept was used to explain an area of anomalously old oceanic crust adjacent to the Mexican margin at the mouth of the G ulf of California, but more recently this concept has been expanded to include late Miocene extensional faulting and marine sediments from areas surrounding the northern and central parts of the Gulf o f California (Ledesma-Vazquez et al., 1997). These extensional structures and sediments are exposed around the Gulf in the “Extensional Gulf Province” (Gastil et al., 1975) on the east side of Baja California and the west coast of mainland Mexico. Stock and Hodges (1989), suggested that late Miocene extension in the Gulf Extensional Province was similar in style to that of the Basin and Range province (Figure 2), but may have kinematically been a component of the Pacific-North America plate boundary displacement. This implies that in late Miocene time, plate boundary displacement occurred both on the borderland faults west of Baja California and on extensional faults east of Baja California isolating the peninsula as a rigid block within the Pacific-North America boundary zone (Nava Sanchez et al., 1998). Baja California is mainly an unextended terrane. Extensional structures are evident only along the eastern margin of Baja California adjacent to the Gulf of California (Axen, 1995). In northern-most Baja California, the eastern margin of the unextended terrane is marked by a conspicuous escarpment (the Main Gulf Escarpment) produced by a single normal fault or a system of closely spaced normal Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 13 COLORADO PLATEAU ENS '•TwA<lEho J t 8 ? PACIFIC PLAT S C O C O S PLATE Figure 2. Baja California peninsula and adjacent mainland North America, showing the southern Basin Range Province and the G ulf Extensional Province. From Stock and Flodges, (1989). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 14 faults. The Main Gulf Escarpment is analogous, as described later, to the eastern escarpment of the Sierra Nevada in Nevada and California. Faulting related to the escarpment spreads out to the south near latitude 30° 15’ N into a zone of numerous high-angle normal faults. The tilting of strata and local detachment faulting in northernmost Baja California are middle and late Miocene or younger in age, and locally this tilting is dated at around 9 to 6 Ma. A small metamorphic core complex is present in the northernmost part of Baja California, about 45 km south of the United States-Mexico border. Farther south in Baja California, near latitude 21° 20’ N, significant strata tilt is seen in 10-20 Ma rocks below flat-lying uppermost Miocene and lower Pliocene strata (Sawlan and Smith, 1984; Stock and Hodges, 1989). In this area, the Main Gulf Escarpment is younger than 10 Ma. Near latitude 26° 45’ N, strata as young as 8 Ma locally dip as much as 45° (Stewart, 1998). 2.2.3 Continental Rifting. The basic structural element of a continental rift is considered to be a “Half Graben” (Ingersoll and Busby, 1995). The single, major fault zone that controls the asymmetrical basin is called the border fault, and border faults may step to the right or left and/or ‘flip” dip direction across transfer faults (Ingersoll and Busby, 1995) (Figure 3). The characteristic structural asymmetry of many continental rift basins and their uplifted flanks exerts a fundamental control on the distribution of sedimentary environments and lithofacies. This is particularly true along the basin margins, where transverse drainage systems evolve on the footwall and hanging wall uplands, Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 15 L a t e r a l flu v ia l . s y s te m aft on i o n Accom T r a n s fe r fa u lt Early syn-rift stage Figure 3. Tectono-sedimentary model of three-dimensional structure and sedimentary environments in early stages of syn-rift evolution of rift basin. From Leeder (1995). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 16 transferring clastic sediment toward the basin center, frequently via alluvial fans and fan deltas (e.g., Zanchi, 1994). The length o f the tectonic slope produced during extension controls the area of newly created tectonic uplands free to be drained by runoff. Drainage-basin area is the primary control on the size of transverse-source alluvial fans that form along graben margins, although climate and bedrock lithologies are important modifying influences. A half graben may thus be envisaged as a sink for introduced clastic sediment and for biogenic and chemical sediments (Leeder, 1995). Both Alfonso Basin in the western slope of the Gulf of California and the eastern slope of Pescadero Basin are products of extensional tectonics in a borderland type margin setting and present us with a unique location for the accumulation of sedimentary sequences. High sediment accumulation rates allow development of sedimentary sequences with millennium to interannual resolution. The site at eastern Pescadero Basin intersects the oxygen minimum zone and the silled nature of Alfonso Basin limits ventilation and promotes anoxic or suboxic conditions, so in both locations the primary sedimentary structures or microfabrics are preserved. These factors and the fact that they are situated in an area influenced by tropical and temperate processes, make these basins ideal for this study. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 17 3. CLIM A TE AND OCEANOGRAPHY 3.1 Climate The mountains in the Baja California Peninsula separate the Gulf from the climate controlling influence of a major ocean. As a result of this and its general configuration, the climate is more characteristic of the continental regions to the east. The influence of the arid conditions of the Sonora desert is more evident during the late fall to early spring months (winter), when strong winds blow from the north. The conditions become more tropical during the summer-early fall (summer) when weaker southerly winds bring in more humid and warmer air (Merrifield and Winant, 1989). The configuration of the elongated and narrow Gulf also affects the pressure systems that control the winds in the region, generating a seasonal surface wind reversal. During the winter season the Aleutians low-pressure center expands and an East Pacific high-pressure center influences the region over the southwest United States and Northeast Pacific ocean. This high-pressure center and an associated low located over the Sonora desert generate strong winds that travel along the axis of the Gulf in a NW-SE direction. During the summer, the Aleutian low contracts and the Sonoran low moves to the head of the G ulf generating weaker winds in the SE-NW direction (Badan-Dangon et al., 1991), a strong thermocline develops and productivity is reduced. This time also brings most of the precipitation to the Gulf; more than 70% of the rain falls between May and October (Douglas et al, 1993). Pares-Sierra et al. (2003) examined the surface winds over the G ulf using satellite- derived data and challenged the idea o f a monsoonal symmetry structure for the Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 18 winds. They found that for the winter months (December, January and February) northwesterly winds with an average magnitude of 4.93 ms' 1 dominate the entire Gulf. By the months of March, April and May the intensity diminishes everywhere. Toward the end o f May the winds weaken further and change direction towards the mainland. In the summer months (June, July and August) the winds have diminished everywhere and attain a northeasterly direction toward the gu lfs oriental coast. Pares-Sierra et al. (2003) also found that the reduction in magnitude and the change in direction for the northern Gulf are a lot less pronounced. The winds in the southern Gulf do reverse for short periods but at the seasonal and monthly scales the winds never reverse direction completely (Figure 4). Air temperatures decrease toward the upper Gulf during the winter months and the temperature contrast between the Pacific and Gulf coasts of Baja California is very small. During the summer, temperature increases over the Gulf and the contrast sometimes exceeds 10°C (Roden, 1964) (Figure 5). 3.2 Water Masses and Circulation Waters at the mouth o f the Gulf o f California lie in a complex oceanographic transition zone where at least six water masses have been detected. In the spring, California Current Water (CCW) spreads across the entrance while in autumn Tropical Surface Water (TSW) is introduced from the Costa Rica Coastal Current (Castro et al., 2000) (Figure 6). CCW is usually confined to the mouth. TSW is present in this region but does penetrate to the central Gulf during El Nino events. At deeper levels Subtropical Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 19 31.Q°N 29.0°N 27,0°N 25.0°N 23.0°N 3 1 .D°N 29.0°N 27.Q°N 25.0°N 23.Q°N 115.0f f W 112.0°W 109.0°W 115,0'W 112.0°W 109.0°W Figure 4. Seasonal surface wind climatology for the December-January (a), March-April-May (b), June-July-August (c) and September-October- November (d) periods. From Pares-Sierra et al. (2003). s s s Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 20 MEAN AIR TEMPERATURE JANUARY (C°) 20 32 MEAN AIR TEMPERATURE JULY (C°) * 2 0 26 • MEAN PERCENTAGE OF SUMMER RAIN MEAN ANNUAL RAINFALL (CM) 20% 30% 20% MAY TO OCTOBER 50 , ,60 % 70% ,2 5 1 ti 50 Figure 5. Gulf of California’s Mean Air Temperature (C°) for the months of January (a) and July (b), and Mean Annual Rainfall (c), and Mean Percentage of Summer Rain, May to October (d). From Roden (1964). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 21 33.8 34.0 34.2 34./* 34.6 34.8 35.0 35.2 SALINITY 0 /0 0 Figure 6 . Temperature and Salinity diagram for CTD soundings at the entrance to the Gulf of California showing water masses present. From Castro et al., (2000). ASE = Tropical Surface Water, AGC = Gulf of California Water, ACC = California Current Water, AsSt = Subtropical Subsurface Water, AIP = Pacific Intermediate Water and APP = Pacific Deep Water. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 22 Subsurface Water (STSsW), Pacific Intermediate Water (PIW) and Pacific Deep W ater (PDW) occur but their limits are difficult to distinguish in TS diagrams since their distinctive characteristics become blurred as they travel north into the central and upper Gulf where evaporative processes transform surface waters into the Gulf of California Water (GCW) which then mixes with the SSW as GCW is advected south (Torres-Orozco, 1993) (Table 1). A four-layer circulation model by Bray (1988) proposes CCW and TSW moving seasonally in and out of the Gulf; outflow of GCW mostly between 50 and 250 m; inflow of STSsW between 250 and 500 m; and inflow of PIW and PDW below 400-500 m (Douglas, 2001). Table 1. Summary of characteristic TS values for the water masses in the Gulf of California. From Torres-Orozco (1993). W ater Mass Denomination Abbreviation Salinity ppm Temperature °C California Current Water CCW <34.5 12-18° Tropical Surface Water TSW 35.0 18-35° Gulf of California Water GCW 35.0 12.0° Subtropical Subsurface Water STSsW 34.5-35 9-18° Pacific Intermediate Water PIW 34.5-34.8 4-9° Pacific Deep Water PDW >34.5 <4° At present Alfonso Basin is located within the La Paz Bay and exchanges water with the Gulf mainly through Boca Grande (Figure 1). Alfonso Basin is only exposed to Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 23 TSW and STSsW and perhaps the CCW since the bathymetric sill (350 m effective depth) obstructs the incursion of PIW and PDW. The other connection with the Gulf via San Lorenzo Channel, is only 20 m deep (Femandez-Barajas et al., 1994; Molina-Cruz et al., 2002). 3.3 Oxygen Minimum Zone The dissolved oxygen concentrations throughout the Gulf of California are high near the surface but rapidly decrease to minimal low values below 200 m. At depths of between -200 and 1100 m, oxygen concentrations are less than 0.3 ml/1 and may be so low as to be undetectable (Alvarez-Borrego and Lara-Lara, 1991; Calvert, 1964; Roden, 1964). The depth range of the oxygen minimum zone (OMZ) varies in the Gulf. North of Tiburon Island there is no OMZ, saturation values are found at the surface. At depths of about 100-150 meters values are still at about 2 ml/1 and are about 1 ml/1 at the basin’s floors due to very active mixing processes mainly because of its shallow characteristics and a very strong tide regimen. Even the deep Ballenas Channel (-1,600 m) has a very oxygenated column with bottom values o f about 1 ml/1. In the Central Gulf, the OMZ is more intensified and extends to greater depths on the east side of the Gulf than on the west (Calvert, 1964; Roden, 1964). Calvert (1964), attributes these spatial differences to higher primary production rates and increased oxygen demand. The OMZ also extends into shallower depths (becomes thicker) towards the mouth (Alvarez-Borrego, 1991). Variations in the upper depth range of the OMZ along the axis of the Gulf reflects a Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 24 combination of factors, including the influence of well oxygenated Gulf Water as it mixes to the south with oxygen-poor Subtropical Subsurface Water. 3.4 Climatic Indices: ENSO, PDO and others. Bemal Franco, (2001), attributes the oceanography of the subtropical Pacific in the northern hemisphere at annual and decadal scales to control by the North Equatorial Current and the North Pacific Gyre, and by the recent oceanic warming. Others believe that it is controlled by the circulation of the Hadley cell due to insolation variability, resulting in changes in the latitudinal position of the Intertropical Convergence Zone (ITCZ) and in the wind patterns (Haug et al., 2001). Sea Surface Temperature (SST) anomalies are in many instances the reflection of major climate changes since such anomalies are caused by wind-driven processes (Schwing, et al. 2002) and researchers have used different indices to document such changes. Among the most recognized are the El Nino-Southern Oscillation Index (ENSO), the Pacific (inter) Decadal Oscillation (PDO) (Mantua et al. 1997), and more recently the Northern Oscillation Index (NOI) (Schwing, et al. 2002). There is a great deal of variability in the oceanographic conditions o f the Pacific Ocean and especially in the Gulf of California. Temporal variability has a wide scale range; it varies from interannual to interdecadal to millennial scales. For the purposes of this study the variability of interest is that within the interdecadal to millennial scales because sampling resolution prohibits detection of sub decadal cycles and the core length (time) limit the observable longer cycles. The cores used in this investigation were sampled every 1 cm, which represents -20 years. The lower end of the Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 25 variability (interannual) is characterized by 3-7 year cycles known as El Nino events and is very well defined by the ENSO (El Nino Southern Oscillation) index. Those of interdecadal variability are characterized by 20-40 year cycles and have been defined by the PDO index (Mantua et al., 1997). Minobe (1997) has shown that 20th century PDO fluctuations were most energetic in two general periodicities, one from 15 to 25 years, and the other from 50 to 70 years. Other periodicities have been recognized at the centennial and millennial scales with rhythms at 350, 900 and l-2k years. In the Gulf, El Nino impacts both the hydrography and productivity. During major El Ninos, the North Equatorial gyre intensifies, pushing tropical surface waters far into the Gulf and restricting the California Current to areas north and west of Baja California. These are times of increased precipitation in the Gulf and over both the mainland and the peninsula region (Salinas-Zavala et al., 1998). Interannual anomalies in sea level in the interior of the Gulf are strongly associated with the ENSO index (Quinn, et al. 1979). This index is based on the seesaw shift in surface air pressure at Darwin, Australia and the South Pacific Island o f Tahiti. When the pressure is high at Darwin it is low at Tahiti and vice versa. El Nino, and its opposite event - La Nina - are the extreme phases of the southern oscillation, with El Nino referring to a warming o f the eastern tropical Pacific, and La Nina a cooling. The PDO index was first introduced by Mantua et al. (1997) who originally identified a pattern of temperature changes associated with the frequency of salmon landings in Alaska, Oregon, Washington and California. A seesaw type of pattern occurs when decades of poor catches in Alaska are represented by good catches in Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. California and vice versa. Latter Mantua and collaborators introduced an index that incorporates data from sea surface temperatures (SST) and sea level pressure (SLP) for the tropics and northern hemisphere, winter north American land surface air temperatures and precipitation, winter northern hemisphere 500 mb height fields, sea surface temperatures for the west coast of north America and stream flow records from western north America (Figure 7). The PDO index was developed based on the empirical orthogonal functions of the SST’s in the northern Pacific, it’s negative mode occurs when temperatures in the north Pacific are similar to those of a La Nina event, that is it is associated with a cool phase. When the PDO is in its positive mode, El Nino events are intensified and are associated with a warming phase. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 27 PDO NPP1 Q. T5 O N "m -SOI o c GTI 2000 1980 1960 1920 1940 1900 0.8 0.4 0.2 0.0 °C - 0.2 -0.4 - 0.6 Figure 7. (top) Normalized winter mean time histories o f Pacific climate indices. Dotted vertical lines are drawn to mark the PDO polarity reversal times in 1925, 1947, and 1977. Positive value bars are filled with black, negative with gray shading, (bottom) SST and SLP (contoured) regressed upon the PDO for the period of 1900-1992. From Mantua, et al. (1997). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 28 4. METHODOLOGY 4.1 Core Collection and Curation. A total of 6 Multicore and Gravity cores recovered from Alfonso and Eastern Pescadero Basins were analyzed for this study (Table 2, Figure 1). Gravity core BAP94-CB was recovered during the PaleoVII cruise aboard the “El Puma” vessel in May, 1994, and gravity core BAP96-CP during the PaleoVIII cruise in June, 1996, also aboard this Mexican research vessel. All other cores (NH01-15GC3, NH01- 15MC1, NH01-26GC1 and NH01-26MC1) were recovered during the CALMEX NH01 cruise in November-December 2001 on board the RV “New Horizon”. The CALMEX cores were taken to Oregon State University’s core facility in Corvallis for archiving purposes and to scan for Gamma Ray Attenuation Porosity Evaluator (GRAPE), Magnetic Susceptibility, and color imagery (In Line Photo Scan). These cores were split and a working half of each taken to the Sediment Laboratory at the University of Southern California for further analyses. All six cores were X-radiographed for micro fabric analysis and sampled at 1 cm intervals. The X-ray positive was analyzed for varve count using a grayscale digital transformation. Other data was also available in the work of Bernal Franco (2001) in the La Paz Basin. She analyzed the biogenic sedimentary components (calcite, biogenic opal, and organic carbon) in box cores and a Kasten core to explore the paleoceanographic potential of the sediments and to make inferences on the observed variability during the past 7,500 years. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 29 Table 2. Core locations, lengths and depths. Table includes CALMEX and BAP cores used in this study and those used by Bemal-Franco (2001). Core Date Recovered Latitude N Longitude W Length (cm) D epth (m) Basin NH01-15GC3 11/27/2001 24°38’ 20.4” 110°35’ 58.8” 308 408 Alfonso NH01-15MC1 11/27/2001 24°38’ 10.8” 110°36’ 3.6” 40 408 Alfonso NH01-26MC1 12/1/2001 24°16’ 42” 108°11’ 40.2” 27 600 Pescadero NH01-26GC1 12/1/2001 24°16’ 40.2” 108°11 ’ 43.8” 379 600 Pescadero BAP96CP 06/1996 24°38’ 7” 110°33’ 14” 212 390 Alfonso BAP94-CB 05/1994 24°38’ 54” 110°34’ 18” 212 391 Alfonso BAP94-9T 05/1994 24° 24’00” 110°06’00” 38 745 La Paz BAP94-9K 05/1994 24° 24’00” 110°06’00” 176 745 La Paz BAP96-CM 06/1996 24°40’48” 110°25’ 12” 38 400 La Paz * Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 30 4.2 Age-Depth Models A requirement in any paleoenvironmental, or paleoclimatic reconstruction, is a well constrained age model that can be used to date and to correlate with other sequences. The ideal situation would be to have an absolute date for each sampled interval in a sedimentary sequence, but would be impractical. Obtaining a robust age model for a cored sequence requires several steps, including establishing sequences, relative age, correlation and absolute age. The latter is perhaps the first step in this process. An age model for Alfonso Basin was constructed based on the previous age models for core CP recovered in Alfonso Basin and the results extrapolate to core NH01-15GC3. In this way, the cored sequences were predicted to be no more than - 10,000 years old and a detailed age-depth model was constructed using a combination of excess 2 1 0 Pb profiles, accelerator mass spectrometry (AMS) radiocarbon dates, and varve counts derived from gray-scale analysis. 71 fl 778 The radioisotope Pb is an intermediate member o f the U decay chain. Airborne 2 2 2 Rn and 2 2 2 Rn in sea water decays to 2 1 0 PB which is readily absorbed onto particulate matter and removed to the sediments (Joshi and Ku, 1979). Once it reaches the sediments it behaves conservatively, that is, it is buried without participating to any measurable extent in interactions between seawater and sediment pore waters. As sediment is buried, 2 1 0 Pb activity decreases. This decrease is interpreted as being the result of radioactive decay of the unsupported 226Ra. The Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 31 method consists of measurements of 2 1 0 Pb at various depths in the core and calculating the excess 2 1 0 Pb from the difference between 2 2 6 Rn and 210Pb. Sedimentation rates can be calculated using the gradient o f the decrease (Joshi and Ku, 1979). 2 1 2 Pb has a half-life of 22 years, which means that the amount of this element in the topmost layer of a sediment core can provide information about the last -1 0 0 yr. Dr. William Berelson performed the 2 1 0 Pb analyses at the Geochemistry Laboratory of the University of Southern California. For older sediments, AMS radiocarbon dates were performed on planktonic and benthic foraminifera. AMS 1 4 C dating differs from conventional 1 4 C dating in that it uses direct carbon isotope analysis by mass separation. The method is fundamentally based on the loss of 1 4 C in an organic substance by radioactive decay whereby the ratio of 1 4 C to total carbon decreases at a defined rate from a uniform initial value. Plants absorb carbon from the atmosphere in the CO2 exchange and maintain carbon isotopic equilibrium with it. Animals reflect the same concentration of 1 4 C as the plants they eat; “you are what you eat”. The dating clock starts when 1 4 C replenishment ceases at death, and the relative concentration of 1 4 C starts declining through radioactive decay (Arnold, 1995). 1 4 C has been used in marine sediments since 1951 and the advantage o f AMS is that it requires very small samples. Radiocarbon dating of milligram samples back to 60 ka has become routine and the accuracy is comparable to the best beta-counting laboratories, which require larger samples (Litherland and Beukens, 1995). A big disadvantage is the high cost of the analysis since there are only few laboratories capable o f performing it. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 32 Age determinations using radiocarbon methods must be corrected for reservoir effects. These generally result from long-term variations of the 1 4 C to 1 2 C ratios in the atmosphere or oceans. Research efforts since the 1970’s have focused on the means of correcting radiocarbon dates by comparing 1 4 C dates to calendar years based on tree ring counting databases. Several calibration tables have been published but perhaps the most comprehensive and current calibration reference is the 1993 volume o f Radiocarbon (Arnold, 1995; Stuvier et al., 1993), which included the calibration software CALIB. This software is continuously upgraded and has become an important tool in radiocarbon dating. In the oceans, reservoir errors arise when CO2 in deep layers do not come in contact with the atmosphere and the 1 4 C is depleted by radioactive decay before organisms incorporate it in their tissues. This results in age determinations older than the real value. This effect is particularly true in regions of high upwelling where deeper, older water is brought to the surface. In this research AMS 1 4 C dates were converted to calendar years using the CALIB 4.4.1 calibration software of (Stuvier and Reimer, 1993) with a delta R of 249 ±18 years. For the ocean reservoir correction, a date of 574 ± 18 years was used obtained for the regional mean from a Rhodolith (Lithothannium crassiusculum) in La Paz (Frantz et al., 2000). AMS analyses were performed at the Livermore National Laboratory and at the USGS National Center in Reston YA. Sedimentation rates were obtained from varve counts based on X-ray positives of sediment slabs. Varves are annual couplets equivalent to tree rings, forming as a result of changing climatic conditions, which generate seasonal Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 33 variability in factors such as productivity and clastic deposition. Varves are preserved in areas of depleted oxygen. The method consists o f X-radiographing slabs from the cores. These X-radiographs are printed as positives and scanned at high resolution. From these scans, a digital gray scale is obtained and individual varves are counted providing a direct measure of elapsed years. Sediments from Alfonso and Eastern Pescadero Basins are mostly laminated, providing an excellent opportunity to apply this technique. All cores were split and cut horizontally into 1.5 cm thick slabs and x-rayed using a Penetrex industrial X-ray apparatus at the sedimentary laboratory at USC. The X-radiographs were printed as positives and then scanned at 600 dpi resolution using an Astra net e5420 flatbed scanner. The X- ray’s positive jpg image was then processed though the NIH-1.06 software to obtain a grayscale digital transformation (Figure 8). The plot value files were imported into Excel and the pixel value number transformed to distance downcore and plotted vs. the grayscale. NIH 1.06 measures changes in optical density, assigning a value ~1 to the whitest areas and values of -256 to the darkest. After a plot of grayscale vs. distance downcore was made, a varve count was manually obtained for every 5 cm segment of record and were transformed to sedimentation rates and expressed as millimeters per year. Douglas et al., (2002b), using this method established an average of 25 light-dark laminations per centimeter or 0.4 mm/couplet for the upper 20 cm of core BAP96-CP. This rate is identical to the accumulation rate based on excess 2 1 0 Pb and the authors concluded that the couplets represent annual Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 34 Gray Scale Light Dark 256 600 650 a 750 800 850 0.4 Dry Bulk Density g/cm2 0.6 0.2 Figure 8. Example of an X- Radiograph along with grayscale and dry bulk density. Section corresponds to the 60-86 cm portion of core NH01-15GC3. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 35 accumulations or varves. Rates obtained in this way were incorporated into the age model. 4.3 Grain Size Analysis As part of a test to discriminate between fluvial and eolic sources and to investigate variability in the southern Gulf of California, grain size distributions and time series for sediments in cores 15 and 26 were determined using a Horiba Laser Grain Size Analyzer (LA-910) at the Environmental Geochemical Laboratory at the Institute of Oceanographic Research of the University of Baja California. The principle used by the LA-910 to measure particle size distribution is angular scattering of light using sources: An ordinary He-Ne laser (632.8 nm) and a Tungsten halogen lamp, which allows for a measurable size range of 0.1 to 1020 pm. The optical system in a laser-diffraction type analyzer condenses the scattering from a laser beam with a condenser lens and forms an image on the ring-shaped detector located at the focal distance. (Kerker, 1969). This instrument measures particle size in microns and uses the Moment Measures Method to calculate the Mean, Median and Standard deviation of the population. A measure of Skewness was obtained by applying Pearson’ s Second Coefficient o f Skewness: Sk - 3(Mean-Median)/ Standard deviation Sediment from each of the 1 cm sampled intervals was dispersed in 10 ml of a solution of sodium hexametaphosphate (3.8g/20 liters) and analyzed. Replicates were analyzed for some of the samples to define method precision. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 36 4.4 Density Profiles (GRAPE) The GRAPE system is designed to determine the density of core material and estimate the porosity of the sediment using several assumptions regarding mineral and liquid specific gravity. Dry Bulk Density (DBD) is the weight of solids (sediments and sea salts) measured after evaporating interstitial water, divided by the initial volume of the sample. Wet Bulk Density (WBD) includes the mass contribution of pore fluids and is the measure estimated by the GRAPE system (Herbert and Mayer, 1991). Density and porosity are useful for examining downcore lithologic changes and in the correlation of multiple cores within a basin. Also, they are necessary for calculating Mass Accumulation Rates, the product of Linear Sedimentation Rates and DBD. In the GRAPE system, a narrow beam of gamma rays is emitted which pass through the core and are detected on the other side. Density is determined by measuring the number of unscattered gamma photons that pass through the core unattenuated (the counter only detects photons which have the same principal energy as the source) and comparing the result to a water-aluminum calibration standard core with known densities. The equation for calculating bulk density from gamma ray attenuation measurements is: WBD = 1/md * ln(Io/I) where: WBD = sediment wet bulk density m = the Compton attenuation coefficient d = the sediment thickness I0 = the gamma source intensity I = the measured intensity of the sample Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 37 Porosity is calculated directly from sediment wet bulk density if the following are known or can be reasonably estimated: a) the sediment is fully saturated, b) the density of the mineral component, and c) the fluid density. Fractional porosity is calculated as follows: FP = (om - WBD)/(am - aw ) Where: FP = fractional porosity am = mineral grain density WBD (or gamma density) = Wet Bulk Density c t w = fluid density Dry Bulk Density is simply calculated as: D BD = (l-FP)am +FP-0.025 Where FP-0.025 is an estimate of the sea salt contribution to mass (Herbert, 1991). 4.5 Mass Accumulation Rates Linear Sedimentation Rates (LSR) and Mass Accumulation Rates (MAR) are temporal measures of sediment accumulation on a substrate. MAR are a measure of flux of material across the sediment/water interface. LSR cannot be used to determine mass flux, it only measures thickness deposited over a time period. A big advantage of using MAR over LSR is the possibility of making comparisons on temporal and areal bases, since it is not affected by variable compaction (Rea and Janecek, 1981). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 38 As stated before, MAR is the product of LSR and DBD and if the proportion of any component of the sediment is known, the MAR of that component is the product of the total MAR and the weight percent of that component (Rea and Janecek, 1981). 4.6 SEDIMENT COMPONENTS Samples were analyzed for carbonate, total carbon, biogenic opal, total organic carbon and terrigenous sediment content (Douglas et al. 2002b; Gonzalez- Yajimovich et al., 2002). 4.6.1 Biogenic Opal Content Biogenic opal was measured using alkaline extraction and the reduction colorimetric technique described in Mortlock and Froelich (1989). A sample weighting between 25 and 50 mg is freeze-dried, powdered, weighed, and placed in a 50-mL centrifuge tube. The sample is then oxidized using a H2O2 solution to remove organic carbon and then calcite is removed using IN E1CL. Twenty milliliters of deionized water is added to each tube, the sample is centrifuged, and the supernatant discarded. A single-step extraction o f Si is performed on the samples using 40 mL of NaOH at 85°C for 5 hr. After centrifugation, 20 mL of the supernatant is transferred to a polyethylene vial and dissolved silica is determined by amolybdate blue spectrometry. Absorbencies are read at 812 nm using a spectrophotometer. Biogenic opal is obtained from these determinations by means of the Mortlock and Froelich (1989) equation: Biogenic Opal (%) = 2.4 x Siopal (%) Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 39 4.6.2 Total Carbon Content Total carbon content was determined for samples of CALMEX cores NH01- 15GC3 and NH01-15MC1 using a Euro Vector Elemental (Euro EA 3000) analyzer at University of Southern California. This instrument is based on the dynamic flush combustion principle coupled with gas chromatography. Precision was established with acetanilide as a standard. For CALMEX cores NH01-26GC1 and NH01-26MC1, total carbon content was determined with a LECO Elemental analyzer (LECO CHNS-932). Precision was established with cystine as a standard. 4.6.3 Total Organic Carbon Content Having obtained inorganic carbon and total carbon as described above, total organic carbon was obtained simply by subtracting the values of inorganic carbon from total carbon. 4.6.4 Carbonate Content Samples were obtained from all cores at 1 cm intervals by cutting a 2 cm piece from a 1 cm thick slab with a spatula, and samples were then dried in a 50 ml beaker at 80°C for a period of 24 hours and then manually pulverized in a mortar. A ~20 mg sub-sample was weighed and analyzed for total inorganic carbon (TIC) in a Carbon Dioxide Coulometer (UIC, Inc. M odel CM5014). To measure TIC contained within the sediment, 5 ml of perchloric acid 2N was used in an acidification module to evolve CO2 from each of the 20 mg samples and the gas was swept into the Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 40 coulometer cell where it was detected and displayed on a digital screen in terms of micrograms of carbon. The coulometer cell is filled with a partially aqueous medium containing ethanolamine and a colorimetric indicator. Carbon dioxide is quantitatively absorbed by the solution and reacts with the ethanolamine to form a titratable acid, which causes the indicator color to fade. Photodetection monitors the change of color in the solution as a percent transmittance. After the process is completed the instrument automatically returns the solution to its original color (blue). Calcium carbonate content was then calculated from the results by using the following equation: which yields carbonate values expressed as weight percent of sediment. 4.7 Eolian Sediment Traps To verify the source o f the terrigenous materials, 5 dust traps were installed in strategic locations around the La Paz Bay: El Coyote, Las Animas, Microondas, Pichilingue and Isla La Ballena. The dust traps chosen for this study were developed by the US Geological Survey (Reheis and Kihl, 1995) and consist of an angel-food cake pan mounted on a steel fence post about 2 meters above the ground (Figure 9). The USGS design includes a wire screen that is fitted just below the top of the pan. Marbles keep the dust that has filtered into the trap from being blown out again. A protective wire over the top o f the cake pan was spread with Tanglefoot®, a commercial sticky substance that discourages birds from perching on the trap. CaCO,Wt.% = 0.8335^C„„W , - ) sample Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 41 Figure 9. Dust trap used. The design developed by the U.S. Geological Survey, consist of an angelfood cake pan mounted on a steel fence post. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 42 4.8 Sediment Trap To qualify the sediment being deposited in Alfonso Basin, subsamples from a sediment trap were obtained and analyzed. Together the results from the sediment trap and on-land dust traps were used to determine the source of the materials entering Alfonso Basin and to evaluate both the source seasonality and the quantity of clay and silt that is preserved in the laminated sediments and in assessing if the dark layers are of eolian or fluvial origin. Sediment traps are conical or cylindrical structures designed to collect sedimentary particles as they settle through the water column on their way to the ocean floor. They are of different configurations and sizes. A Technicap PPS-3/3 model trap deployed at 24°38’ N, 110°35’ W and moored so that it collected at a depth of 350 m was used to collect the samples (Silverberg et al. 2003). This trap model has an aperture of 1/8 m2 and can be programmed to collect for periods of days to months in a 12-bottle carousel (Figures 10 and 11). The trap was programmed to collect one week samples, and subsamples for the periods of August 7-Nov 1, 2002 and August 23-Oct 3, 2003 were available and used in this investigations. 4.9 X-Ray Diffraction X-ray diffraction was performed on sediments from cores 15GC3 and 26GC1, on sediments from the dust traps, coastal dunes, the marine sediment trap, and on sediment samples from five arroyos draining the region; El Coyote, San Juan, Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 43 310 m subsurface floats 160 k hydrographic cable, 50 m 360 m Sediment Tramp Technicap PPS 3/3 1/8 m2 aperture swivel hydrographic cable, 45 m ground line 1000 rn acoustic release V i Chain 500 k 50 k Figure 10. Schematic diagram showing Alfonso Basin’s sediment trap mooring. A Technicap Sediment Trap Model PPS-3/3 (1/8 m2 aperture) was used. From Silverberg et al., (2003). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 44 Figure 11. Technicap PPS-3/3 sediment trap on deck on the BO Ulloa after recovery. Photo courtesy of Fernando Aguirre Bahena. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 45 Loreto, Santa Rosalia, and La Giganta. Samples from core 26GC1 were obtained at every 25 cm and those from 15GC3 at every 50 cm. A 63 pm sieve was used to remove the coarse fraction of the sediment and the remaining fines were macerated in a agate mortar. Acetone was added to the macerated material and the mixture was transferred to a glass slide using a Pasteur Pipette and allowed to air dry. In this way, a thin surface of approximate 24x24 mm was produced and analyzed in a Rigaku™ XRD scanner. In this way mineralogy was obtained. 4.10 Spectral Analysis. Spectral analysis was performed of sediment components and grain size analysis in all cores. The analyses were performed applying the Multi-Taper Method (MTM) on Matlab® 6.5 and used to identify millennial and centennial peaks of ocean-climate variability in the Gulf. A compilation o f all peaks significant at the 5% level (95% confidence level) was completed separating two large groups; one that included biological productivity proxies and another that included rainfall proxies. Most records were analyzed using three tapers, which give good frequency resolution for decadal and longer scale variability. No filters were applied in the process. Content weight % records were used for the sediment components, and for the grain size series, data was entered in microns. The resulting power spectra frequency peaks were converted to calendar years based on the age-depth models. Only the peaks with multiple repetitions among the records were considered and then only those present in all locations. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 46 5. ALFONSO AND EASTERN PESCADERO BASINS SEDIMENTARY RECORD. 5.1 Review and Previous Work. Modem slope basins contain sedimentary accumulations dominated by a) terrigenous sediments; (b) biogenic sediments, and on the slopes and basal plains of some low oxygen basins laminated sediments (Figure 12). The main component of the sediments of Alfonso Basin is terrigenous mud (>80%) (Douglas et al., 2002b). Such materials are the product o f continental erosion and find their way to slope or abyssal basins through drainage basins, alluvial fans, transitional environments and delta systems. Nava-Sanchez (1997), based on 3.5 KHz seismic profile records and box cores, found that sediments from the San Juan and El Coyote fan deltas bypass the slope and are deposited at the slope base or in Alfonso Basin. As a silled depression, Alfonso Basin captures most of the fluvially derived terrigenous contribution as turbidity current and flood plumes. Hemipelagic infall is also an important source of sediment. Molina-Cruz et al. (2002) proposed that the terrigenous input to the Bay o f La Paz is regulated by pluvial runoff and that it’s fluctuations follow the frequency o f sunspot cycles. A potential source o f the terrigenous sediment is eolian derived material. The wind regime in the La Paz Bay region during the winter-spring months is from the NW while during the summer-fall months the wind regime is from the SE (Thunell et al. 1996). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 47 San Jose island San Frandsquito Island Mas Alia del Espkitu Santo Bank Lobos Basin Esplritu Santo Z~J LA PAZ CITY 800 LA GiGANTA RANGE PROFILE A-B GULF OF _________CALIFORNIA v pelagic s*fimW*atk>n i 'Bank, LA PAZ BA Y sediments L O B O S t _b a s i n _ ALFONSO BASIN. Figure 12. Bathymetric chart of La Paz Bay and Morphological section showing the structure and position of Alfonso basin as well as the general sedimentation patterns. Contours every 50 meters. After Nava Sanchez, (1997). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 48 The rainy season begins in the late summer-early fall (Bernal Franco, 2001), so during the early summer months conditions are dry and windy and more conducive to eolian transport. These conditions can be extended during periods of drought related to La Nina conditions. Thus, the proportion of eolian sediments in the terrigenous record is an indicator of dry conditions. The variability in sedimentation rates in the basin, 0.32 to 0.52 mm/yr, average 0.41 mm/yr, may be related to ENSO events. Hemipelagic sediments are mainly composed of biogenic material derived in the water column and minerals are normally present in relatively small quantities (Bernal Franco, 2001). The biogenic material is carbonate (foraminifers and coccolithophorids) and biogenic opal (diatoms and radiolarians) shells and organic debris produced in surface waters. Sedimentation in Alfonso Basin occurs in two seasonal modes 1) Terrigenous (fluvial and eolian) during the summer season and 2) Biogenic (diatoms, foraminifers and coccolithophorids) during the winter and spring (upwelling) seasons. These conditions generate laminated sediments that are preserved on the basin slope wherever it intersects the oxygen minimum zone. Byrne and Emery (1960) in one o f the earliest investigations of the sediments in the Gulf of California, analyzed samples collected during cruises VII and XVI of the RV “Scripps” in 1939 and 1940, respectively. They described the northern Gulf sediments as deltaic; the central region as composed of mainly siliceous Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 49 (diatomaceous) mud produced by strong upwelling and high nutrient conditions from northwesterly winds generated during the winter season; the southern region was found to be composed of marine green mud. Along the coastal areas are sand and gravel composed of detritus from land and shell fragments, van Andel’s (1964) monumental work on the sediment sources and their dispersal patterns focused on the heavy mineral content in order to define provenance. He concluded that the northern Gulf (from the delta to Tiburon Island) was composed of Colorado River sediments and named this region the “Colorado River Sedimentary Province” based on the homblende-epidote-pyroxene mineralogical suite that is characteristic of Colorado River sediments. The central and southern regions receive sediment from discharges of land adjacent to the Gulf. The dispersal of the deltaic sediments is predominantly in a north-south fashion whereas in the central and southern regions the trend is from the margins to the basins, directly seaward of individual river sources. The eastern side has developed wide margins because o f the several drainages that contribute sediment. The western margins have less sediment and in areas of very low terrigenous input, calcarenites dominate. Basin sediments in the central region are composed mainly of diatomites whereas in the south they are very fine-grained terrigenous sediments and the opal is mainly radiolarians. Byrne and Emery (1960) also reported the occurrence o f laminated sediments in the Gulf and offered one of the first explanations of their origin, i.e. that the light members represent concentrations of diatoms resulting from plankton blooms during winter upwelling (seasonal pulses) imprinted over a steady deposition of terrigenous silt and Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 50 clay. They suggest that a couplet of the resulting lamina represents a year’s sedimentation cycle. Calvert (1964) argued that varves are formed by superimposing a summer pulse of terrigenous silts and clays on a steady supply of organic detritus, but agreed that the couplets represent an annual cycle. Baumgartner et al. (1991b) established a well constrained record of the dark lamina from 1934 to 1966 and demonstrated that the construction of dams on major rivers in Sonora that began in the 1940s, did not have any effect in the accumulation of the varves. They proposed that the terrigenous input occurs mainly through eolian processes by removal and transport of desert dust associated with convective summer thunderstorms. Work by Pike and Kemp (1997) shows that Calvert’s argument for steady production of phytoplankton is an oversimplification. The composition and origin of the laminations in the sediments of Alfonso Basin appear to be different from those studied elsewhere, including those in other locations in the Gulf of California. Laminations in the Gulf can be categorized as two different types based on their appearance, thickness, composition and formation. The first type is a “Guaymas-Type” and refers to those described in the previous discussion. These laminations are almost straight and have a very clear and contrasting definition. They are common in the central Gulf. The second types are those found in the southern Gulf along the west side and especially in Alfonso Basin (hence the “Alfonso-Type” name), here the laminations are not sharply defined, rather they are thin and wavy in appearance and the boundary between them is Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. commonly diffuse. In X-radiographs individual dark-light couplets are difficult to differentiate to the naked eye and easy to omit during counting (Figure 13). Because of the much higher accumulation rates, couplet thickness in Guaymas-type laminations are typically 1-3 mm whereas in Alfonso-type they less than 0.5 mm. In Alfonso-type laminations diatoms occur in low number, especially mat-forming ones, that give structure to the lamina. In this basin, bacterial mats may be the cause for the “wavy” lamination (Douglas et al., 2002a; Staines-Urias and Douglas, 2004). Baba et al. (1991) sampled 87 locations to identify the sources and dispersal of sediments in the Gulf and described sediment patterns similar to those described by van Andel (1964). A factor analysis of sediment bulk chemistry of surface sediment describe four end members: terrigenous elastics, biogenic opal, biogenic carbonate and manganese-rich components. Terrigenous sediments account for 80 to 90% of the total sedimentation on the eastern margin of the central and southern Gulf but less than 40% on the western margin. They calculated mass accumulation rates of the terrigenous component on nine laminated cores and found that rates on the eastern margin are three to five times higher than those on the western margin. Baba et al. (1991) also performed quantitative X-ray diffraction studies on clays (2-4 pm size fraction) and identified distinct mineralogical provinces based on the quartz:feldspar ratios and on anorthite content o f the plagioclase feldspars. The highest values (Q/F=0.74) were found to correspond to the northern Gulf and they decrease southward in most of the Gulf. A n exception is the western margin between Santa Rosalia and south of Loreto where the very low values (Q/F=0.21) indicate that the Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. a) Guaymas type b) Alfonso type Figure 13. X-Radiographs of sediments from the Gulf of California. A) Guaymas- type laminations. Sharp contrasting lamina characterizes this sediment. B) Alfonso- type laminations characterized by wavy and sometimes discontinuous boundaries. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 53 sediments are derived from the basic igneous rocks of Baja California. The northern G ulf clays are dominated by Colorado River clays and the central and southern Gulf have the same types of clays as the geologic provinces on the Mexican mainland. Baja California is only a minor contributor to the western shelves and upper slopes. In 1979 the DSDP drilled 4 cores at the mouth o f the Gulf of California and the sediments obtained consisted of hemipelagic clays and silts that were examined by semi-quantitative X-ray diffraction to determine their mineralogy (Schumann, 1983). The clays consist of smectite with subordinate illite, chlorite, and kaolinite and minor clinoptilolite. Schumann found that quartz and feldspar are invariably present in the silt fraction and carbonate is present at all sites. 5.2 Results 5.2.1 Age-Depth Models Core BAP96-CP.- Based on three different methods, an average sedimentation rate of 0.27 mm/year was obtained for this core. Radiocarbon dates at core intervals 0-1 cm, 120-121 cm and 211-212 cm based on mixed planktonic species (Douglas et al., 2002b) and for intervals 19-20 cm, 100-101 cm and 210-211 cm based on mixed benthic species (Perez-Cruz, 2000) were obtained for this core. The resulting age-depth profile formed a linear relationship (r=0.997) supporting the observation from X-radiograph stratigraphy that sedimentation was continuous below 5.5 cm. The sedimentation rates, interpolated between calendar-calibrated radiocarbon dates, range from 0.32 mm/yr near the top o f the core to 0.24 mm/yr Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 54 below 120 cm (Figure 14). For the core top, excess 210 Pb and 1 3 7 Cs profiles were obtained and yielded a rate of 0.4 mm/yr. Gray scale analysis for the upper 20 cm o f the core averaged about 25 light- dark laminations per cm, or 0.4 mm/couplet, identical to the accumulation rate based on the excess 2 1 0 Pb profile. Below 20 cm, sedimentation rates vary in a cyclic fashion from 0.32 to 0.52 mm/yr and average 0.41 mm/yr, very close to modem rates. Below 150 cm, laminations are thinner, often disrupted and more difficult to discriminate, and the record contains an increased number o f flood and turbidite layers (Gorsline et al., 2000). Accumulation rates in this interval range between 0.23 to 0.27 mm/yr (Appendix A). Considering the spacing of radiocarbon dates and that the core has been compacted due to dissolution of siliceous and carbonate debris, the rates based on the three methods are in reasonable agreement. Both the radiocarbon-based rates and varve-count rates indicate that below 150 cm, prior to 5200 yrs BP, accumulation rates in Alfonso Basin based on this core were significantly lower (Douglas et al., 2002b). Core BAP94-CB. The Age model for core BAP94-CB was obtained by correlating the carbonate content o f cores CB and CP and by gray scale analysis. Both curves have a similar pattern of peaks at, or very near to the radiocarbon-dated horizons and were used as tie-points. A total of seven tie-points were used to prepare CB’s age model (Figure 15). Gray scale analysis for the upper 15 cm of the core, averaged about 40 light-dark laminations per cm, or 0.25 mm/couplet. The upper Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Distance Downcore (cm) 55 Age Model for BAP96-CP based on 1 4 C and 2 1 0 PB Years Before Present (YBP) 150 YBP, 5 cm 812 YBP, 20 cm 40 100 3226 YBP, 102 cm 120 3976 YBP, 121 cm 140 160 180 7535 YBP, 210 cm 200 7770 YBP, 212 cm 220 8000 6000 2000 4000 0 Figure 14. Age Model for Alfonso Basin (station BAP96-CP) based on Radiocarbon calibrated and excess 2 1 0 Pb data. Data from Douglas et. al 2002. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Distance Downcore (cm) 56 Age Model for BAP94-CB Based on correlation with BAP96-CP Years Before Present (YBP) 714 YBP, 24 cm 1730 YBP, 60 cm 100 3760 YBP, 110 cm 120 140 4600 YBP, 145 cm 160 180 6680 YBP, 185 cm— 7360 YBP, 201 cm 200 7680 YBP, 210 cm 220 8000 6000 4000 2000 0 Figure 15. Age Model for Alfonso Basin (BAP94-CB) station based on correlation with core BAP96-CP. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 57 5 cm o f this core were lost during coring, so values for the upper 15 cm should be considered as the upper 20 cm. Below 20 cm, sedimentation rates vary in a cyclic fashion similar to core CP but with much lower amplitude. Rates vary from 0.23 to 0.44 mm/yr and average 0.28 mm/yr. Throughout core CB, laminations are very well preserved and easy to discriminate. As in core CP, the record contains a number of flood and turbidite layers but varves seem to be better preserved in this core. Accumulation rates below 130 cm range between 0.24 to 0.3 mm/yr and increased after this time. There is very good agreement between the correlated age model for core CB and the sedimentation rates obtained with the gray scale varve count. Using the average varve count sedimentation rate of 0.28 mm/year, an age of 7500 years is obtained. An age of 7680 years was obtained for this same horizon with the correlated age model. Cores CALMEX NH01-15GC3 and M CI. - An integration approach was used in these cores to obtain sedimentation rates based on corrected radiocarbon dates, excess 2 1 0 Pb profiles and gray scale varve counts. For the 14C-based rates, radiocarbon dates were obtained for the 38 cm, 112 cm, 175 cm, 276 cm, and 308 cm (core catcher) horizons (Table 3). Cores depths for the 15GC3 dates were corrected by adding 11 cm, so they become 123 cm, 186 cm, 287 cm and 319 cm. A rate was calculated for the top 38 cm using a corrected date of 696 YBP and obtained a sedimentation rate o f 0.55 mm/year. The interval between 38 cm and 123 cm (using a corrected 123 cm date o f 2781 YBP) produced a Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 58 Table 3. Result of radiocarbon dating for CALMEX cores used in this investigation. Calibration was done using the CALEB 4.4.1 database of Stuvier and Reimer., (1993). Reservoir age used was 574±18 based on Frantz et al., 2000. Last column shows dates standardized to 2000 AD (+50years). Dates for core NH01-15GC3 (CC) were discarded. Core Interval Planktonic or Benthonic Water Depth (m) l4C age Calibrated Age* Yrs BP Reservoir effect** corrected To 2000 15MC1 37-38 B 408 1920±40 1220±77 646±77 696±77 15GC3 111-112 P 408 3690±60 3,305±146 2731±146 2781±146 15GC3 111-112 B 408 3990±60 3,659±164 3085±164 3135±164 15GC3 174-175 B 408 5030±50 5050±180 4476±180 4526±180 15GC3 275-276 P 408 5130±50 5,166±145 4592±145 4642±145 15GC3 275-276 B 408 5460±40 5,559±89 4985±89 5035±89 15GC3 CC P 408 4655±45 4,556±137 3982±137 4032±137 15GC3 CC B 408 4535±4Q 4,392±119 3818±119 3868±119 26GC2 CC P 600 8760±50 8,920±96 8346±96 8396±96 26GC2 CC B 600 9205±45 9,170±68 8596±68 8646±68 26GC1 CC B 600 9220±60 9607±231 9033±231 9083±231 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 59 sedimentation rate of 0.41 mm/year. The interval between 123 cm and 186 cm (using a corrected 186 cm date of 4526 YBP) produced a sedimentation rate of 0.36 mm/year The interval between 186 cm and 287 cm includes a large turbidite. This event deposited ~81 cm of material between the 282 cm and 201 cm levels and it represents a small time interval. This 81 cm interval was not considered in the calculation of the sedimentation rates for the 186-287 cm interval. The result was a 0.39 mm/year rate. An average rate of 1.34 mm/year was obtained for the upper 40 cm of the core using excess 2 1 0 Pb profiles, but based on isotopic results this is suspect (R. Douglas unpublished data) and appears to be valid only for the first 10 cm. Gray scale varve counts varied between 0.34 and 2 mm/year, averaging 0.78 mm/year. The X-ray/grayscale record for this core showed several blank areas or areas where laminations were impossible to discriminate, so the varve counts became very small and consequently sedimentation rates very high. If these are neglected, then the average rate becomes 0.6 mm/year Using these values a best guess compromise was obtained and a curve was plotted and fitted with a linear regression, obtaining an equation to predict rates through the core (mm/year=-0.0002x (distance downcore cm)+ 0.5614), e.g. 213 cm predicts a rate o f 0.5188 mm/year. From this, an average rate of 0.54 mm/year or 18.51 years/cm was obtained (Figure 16). Cores CALMEX NH01-26GC1 and M CI.- For Eastern Pescadero Basin cores varve counts and two stratigraphic levels were used (350 and 408 cm) and dates are Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Distance Downcore (cm) 60 Age Model for NH01-15 Based on 1 4 C and 2 1 0 Pb Years Before Present (YBP) 93.6 YBP, 11cm 696 YBP, 38cm 40 100 120 3135 YBP, 123cm 140 160 180 4920.4 YBP, 201 cm 200 220 240 260 4921 YBP, 282 cm 280 5035 YBP, 287 cm 300 5767 YBP, 319 cm 320 5000 6000 3000 4000 1000 2000 0 Figure 16. Age model for Alfonso Basin (CALMEX NH01-15) station based on radiocarbon calibrated and excess 210Pb data. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 61 interpolated to the present. (Figure 17). Varve counts range from 0.26-2.94 mm/year averaging 0.80 mm/year. Based on the one radiocarbon date, the average sedimentation rate for eastern Pescadero Basin is 0.41 mm/year, which is consistent with earlier determinations by Baba et al. (1991) and van Andel (1964). Radiocarbon determinations of more levels are pending. Excess 2 1 0 Pb profiles yielded a sedimentation rate of 3.35 mm/year. However there is considerable scatter and this rate far exceeds rates from similar sedimentary settings in the Gulf. Based on others cores, we found 2 1 0 Pb rates to be too high compared to rates based on counts of 14C. 5.2.2 Grain Size Analysis. Mean, Median, Standard Deviation (sorting) and Skewness were obtained for both Alfonso and Eastern Pescadero Basins. In general terms, Alfonso Basin sediments are coarser than those of eastern Pescadero Basin and have wider variability amplitude (Appendix B). Alfonso Basin. - Based in a composite record o f cores CALMEX NH01- 15GC3 and NH01-15MC1, the median grain size is 12 microns average, with a standard deviation of 2.6. Minimum and maximum values are 7.1 and 20.8 microns respectively (Figure 18). Replicate analysis o f this data shows an average error of 13.4% and a standard deviation of 11.4. M ean grain size values range from 11.8 to 139.4 microns, with a 26.1 microns average and 14.5 standard deviation (Figure 19). Replicate analysis shows an average error o f 24% and a standard deviation o f 17. Sorting values (standard deviation) range from 10.8 to 237.9, with an average of 41.2 and a standard deviation of 32.8 (Figure 20). Replicates produce errors averaging Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Distance Downcore (cm) 62 Age Model for NH01-26 Based on 1 4 C Years Before Present (YBP) 120 160 200 240 280 320 : 8682 YBP, 350 cm 360 9083 YBP, 390 cm— < 400 4000 8000 2000 6000 0 Figure 17. Age model for East Pescadero Basin (CALMEX NH01-26) station based on radiocarbon calibrated data. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Downcore distance (cm) 63 Grain Size CALMEX NH01-15 Median Grain Size (microns) 6 8 10 12 14 16 18 20 22 1000 2000 100 3000 150 4000 5000 200 6000 Figure 18. Median grain size downcore for CALMEX NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf o f California. An 81cm turbidite has been removed from the record, see text for explanation. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Downcore distance (cm) 64 Grain Size CALMEX NH01-15 Mean Grain Size (microns) 1000 100 1000 2000 100 3000 150 4000 5000 200 6000 Figure 19. Mean grain size downcore for CALMEX NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. An 81cm turbidite has been removed from the record, see text for explanation. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 65 Grain Size CALMEX NH01-15 a < D 1 -4 — > < D J — < O o a £ o Q 1 0 Standard Deviation 100 0 50 100 150 200 1000 0 1000 2000 3000 4000 5000 6000 Figure 20. Grains size standard deviation downcore for CALMEX NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf o f California. An 81cm turbidite has been removed from the record, see text for explanation. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 66 36% with a standard deviation of 29. Alfonso Basin record shows three very distinct episodes where grain size is coarser and poorly sorted: -1700-1900 YBP, -4000- 4200 YBP and -5400-5800 YBP. These episodes probably represent turbidites. Core NH01-15GC3 included a very large turbidite event from 271 to 190 cm (4921 YBP). The average median for this turbidite is 14.3 microns and the standard deviation for the median 1.4, for the mean, the average is 26.8 microns and its standard deviation 4.3 and for the sorting the average is 36.6 and its standard deviation 12.0. The 81 cm turbidite was excluded from the record for interpretations. Eastern Pescadero Basin. - A composite record o f cores CALMEX NH01- 26GC1 and NH01-26MC1 indicate the median grain size is 5.9 microns average, with a standard deviation of 1.3. Minimum and maximum values are 3.4 and 10.9 microns respectively (Figure 21). Replicate analysis of this data shows an average error of 12.6 % and a standard deviation of 8.24. Mean grain size values range from 6.7 to 29.9 microns, with a 12.9 microns average and 3.1 standard deviation (Figure 22), the average error iss 16.6% and standard deviation is 14.4. Sorting values (standard deviation) range from 7.7 to 50.6, with an average o f 22.3 and a standard deviation of 8.5 (Figure 23), and average error of 36.5% with a standard deviation of 26.62. The basin’s record also shows episodes were grain size is coarser and poorly sorted: -1550-1950 YBP, -3700-4200 YBP, -5200-6000 YBP, and -6900-7500 YBP, in close agreement with the NH01-15 record. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Downcore Distance (cm) 67 Grain Size CALMEX NH01-26 Median Grain Size (microns) 0 50 100 150 200 250 300 350 400 10 11 6 8 9 3 4 5 7 1000 2000 3000 4000 5000 6000 7000 8000 9000 10000 Figure 21. Median grain size downcore plot for CALMEX NH01-26 composite core (GC1 and M CI), eastern Pescadero Basin, Gulf o f California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 68 Grain Size CALMEX NH01-26 Mean Grain Size (microns) 0 1000 2000 3000 4000 5000 6000 7000 8000 9000 10000 5 10 15 20 25 30 Figure 22. Mean grain size downcore plot for CALMEX NH01-26 composite core (GC1 and M CI), eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. g O o 0 C h c j ti Q L - c 1 o Q 50 100 150 200 250 300 350 Years BP Downcore Distance (cm) 69 Grain Size CALMEX NH01-26 Standard Deviation 1000 2000 100 3000 150 4000 5000 200 6000 250 7000 300 8000 350 9000 10000 400 40 50 60 20 30 0 10 Figure 23. Grain size standard deviation downcore plot for CALMEX NH01-26 composite core (GC1 and M CI), East Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 70 5.2.3 Density, Porosity and Mass Accumulation Rates (MAR) Dry Bulk Density (DBD), Porosity and Total MAR were obtained for cores CP, NH01-15 (Alfonso Basin) and NH01-26 (eastern Pescadero Basin) (Appendix C). In Alfonso Basin DBD prior to 3800 YBP is variable but centers at -0.43 g/cm3, after this time and until 300 YBP density varies in a linear fashion from 0.43 g/cm3 to 0.3 g/cm3. After 300 YBP there is a sharp increase to 0.38 g/cm3 and then a decrease to present values. Porosity values decrease in an almost linear fashion from 0.83 to 0.9 at 300 YBP and at this time there is a drastic reduction and then an increase to present values (Figure 24). Total MAR for core 15 is considerably higher and more variable prior to 3800 YBP, during this period the shifts have wide amplitude but the trend is constant at 19 mg/cm2/year. After 3800 YBP, total MAR declined in a step-like fashion from 19 to 10.5 mg/cm2 /year until ca. 350 YBP. After 350 YBP there is a sharp increase to 14 mg/cm2 /year and then a decline to present values (Figure 25). In eastern Pescadero Basin, DBD prior to 6000 YBP is variable but centers at a value of -0.6 g/cm3, after this time and until ca. 4200 YBP density varies in a linear fashion to 0.55 g/cm3. At 4200 YBP there is a sharp decline, a quick recovery and a steady decline to 0.4 g/cm3 at ca. 300 YBP. After 300 YBP there is a sharp increase to 0.56 g/cm3 and then a decrease to present values. Porosity values decrease at an almost linear fashion from 0.75 to 0.85 at ca. 450 YBP and at this time there is a sharp reduction and then an increase to present values (Figure 26). Total Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Downcore Distance (cm) 71 Dry Bulk Density and Porosity NH01-15 0 1000 50 2000 100 3000 150 4000 5000 200 Porosity Dry Bulk Density g/cm3 6000 0.6 0.8 0 .2 0.4 Figure 24. Dry bulk density and porosity in CALMEX NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Downcore Distance (cm) 72 CALMEX NH01-15 Total MAR mg/cm2 /year 1000 2000 100 3000 150 4000 2 0 0 5000 6000 250 2 0 25 10 15 5 Figure 25. Total Mass Accumulation Rates for NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Years BP 73 Dry Bulk Density and Porosity in NH01-26 Porosity DBD g/cm 2000 4000 6000 8000 10000 0.2 0.3 0.4 0.5 0.6 0.7 0.8 0.9 1 Figure 26. Dry bulk density and porosity in CALMEX NH01-26 composite core (GC1 and M CI), eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 74 MAR for core 26 is higher and before 7500 YBP, during this period the shifts have a constant trend centered at 24 mg/cm2/year. After 7500 YBP, total MAR declined in a step-like fashion from 24 to 22 mg/cm2 /year until ca. 4300 YBP (Figure 27). After a sharp decline to 14 mg/cm2 /year and a quick recovery, MAR declines in a constant trend to 17 mg/cm2 /year at ca 470 YBP, another quick recovery to -24 mg/cm2/year, 'j and then a decline to present values (-2 1 mg/cm /year). Molina-Cruz et al. (2002), found that the couplets for core CP were 3.35 mm average thickness, a values that represents a period of 11.2 years in their age model for this location. Results from this investigation show that the couplets represent a one-year period. Molina-Cruz et al. (2002), used electronic scans o f photographs to obtain digital grayscale values, a method not as effective as the use of positive photographs from X-radiographs, which discriminate much finer lamina (Baumgartner et al. 1991a; De Diego and Douglas, 1999). It is possible that their method underestimates the number of couplets. Bernal Franco (2001) used the same methodology as this study and mentioned that based on evidence the couplets could be annual, however her results show that she found the couplets to represent 1-5 years. The difference perhaps is due to the lower sedimentation rates in La Paz Basin and the fact that sediments contain more opal and less terrigenous material resulting in less contrasting lamina. The lack of definition in the very fine lamina could also result in underestimation of the number of couplets. Sedimentation rates obtained in this study averaged 0.54 mm/year for core NFI01-15, Douglas et al. (2002b) obtained an average rate of 0.4 mm/year for core Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Downcore Distance (cm) 75 Calm ex NH01-26 Total MAR mg/cm2 /year 0 50 2000 100 150 4000 2 0 0 6000 250 300 8000 350 10000 400 26 28 2 0 22 24 18 14 16 Figure 27. Total mass accumulation rates for NH01-26 composite core (GC1 and M CI), eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 76 CP and Bernal Franco (2001) obtained rates of 0.39 mm year for core CM and 0.29 mm/year for core 9T, these values show an inverse relationship with location distance from the peninsula confirming the model proposed by Nava-Sanchez (1997) in which the inverse slope generated in a silled basin traps most of the sediment generated by floods and turbidites. Molina-Cruz et al. (2002) pointed out that the most prominent feature of the circulation of the La Paz Bay is a cyclonic gyre fed by Tropical Surface Water and Subsurface Subtropical Water entering the bay across Boca Grande. This circulation pattern could aid gravity in driving hemipelagic sediment toward the center of the basin. Sedimentation rates through the Holocene time increase in CP and CB but the opposite is true for the deepest part of the basin (NH01-15), an effect of sediment focusing. As the basin continues to fill, depth contrast between the core locations is reduced and the sedimentation rates tend to converge. Amplitude of the variation in sedimentation rates is also larger for core NH01-15 and perhaps reflects the concentration of the turbidites as they are deposited in the basin acting as a funnel. Evidence for the focusing in the center of the basin is provided by the thickness of turbidities, e.g. a 81 cm event identified in the center of the basin (core NH01- 15GC3) can be correlated to 2.5 cm thick events reported by Gorsline et al., (2000), in both CP and CB cores. Based on the variations in sedimentation rates it can be concluded that the trend between the eastern slope at CP-CB and the deepest part of Alfonso Basin (NH01-15) is a local effect and that sediment flux in general has decreased in the last Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 77 8000 years. A comparison o f the total mass accumulation for cores NHQ1-15 (Alfonso Basin) and NH01-26 (eastern Pescadero Basin) show almost agreement (Figure 28), suggesting that similar processes act across the southern Gulf region and the trends are Gulf-wide. 5.2.4 Terrigenous Sediment for all cores The amount of terrigenous mud in a deposit is an indirect indication of the amount of rainfall and/or wind intensity. An increase in the amount of wind- transported sediments indicates an intensification of the wind and dryer climate. In the western United States and eastern Pacific Ocean, extended dry conditions are associated with the cooler phase of ENSO and PDO events. High eolian rates would represent a prolonged cold mode monsoon, a condition similar to a cold phase (negative) PDO. If the sediments are predominantly of fluvial origin (hemipelagic) this implicates a more humid regimen in which the adjacent rivers on the eastern margin and ephemeral streams (arroyos) in La Paz Bay provide the bulk of the sediment to the basin. Thus it is clear that the first step in reconstructing paleoclimate in this region is to determine the origin o f the lithologic component. To discriminate between fluvial and eolian materials, five dust traps were installed in strategic locations around La Paz Bay. The sediments were analyzed for composition using XRD techniques and fluxes were estimated and compared to those obtained by Silverberg et al. (2003) with a sediment trap in Alfonso Basin. X-ray diffxactograms were prepared for the samples from core NH01-15, the dust traps, the sediment trap, and from the arroyos around the La Paz Bay. A mineralogical Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Downcore Distance (cm) 78 Total MAR 15 and 26 mg/cm2 /year 0 5 10 15 20 25 30 0 50 2000 100 150 4000 2 0 0 NH01-15 6000 250 300 8000 350 NH01-26 10000 400 Figure 28. Ten point running average of Total Mass Accumulation Rates for cores NH01-15 and NH01-26. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years Before Present description for each was prepared and then compared. The results from core NH01- 15 is the same throughout the length of the record (Figures 29-31), suggesting that the sediment source has not changed through the Holocene. The non-biogenic minerals present in the samples from core NH01-15 are quartz, magnetite, amphibole, pyroxene and an-rich feldspar. Samples from El Coyote and San Juan fans (Figure 32) are mostly pyroxene, with significant amounts of magnetite, quartz and amphibole with minor An-rich feldspar. The difffactograms for these samples are nearly identical to those of cores NH01-15, suggesting that the nearby arroyos are the main source of the terrigenous sediment in Alfonso Basin. These results are consistent with the expected weathering products of the surrounding siliceous tuffs described by Flausback, (1984). Sediments from the Isla Ballena dust trap were mostly with significant amounts of calcite and halite and minor feldspar and pyroxene and stilpnomalane (a layered silicate related to biotite and metamorphism) (Figure 33). The other four dust traps recovered insufficient material to analyze by XRD. Stilpnomalane was not found in any o f the samples from Alfonso Basin and the diffractograms from the dust traps were different from those of core NH01-15, perhaps because the contribution of the eolic component is very small and the dominant contributor dilutes it. The dust traps around La Paz Bay were in place from April 6, 2002 to August 8, 2003 and were sampled at four periods. The period dates, amounts of sediment recovered and calculated fluxes are shown in Appendix D. Excluding periods in which no sediment was found in the traps the minimum sediment capture was 0.087 g and the maximum 0.912 g. This maximum was Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Intensity 80 XRD Core NH01-15 700 700 M Magnetite A Amphibole P Pyroxene Q Quartz F Feldspar (An rich) 600 600 500 500 400 400 300 300 2 0 0 2 0 0 100 100 70 30 40 50 60 10 20 0 Two Theta Figure 29. X-ray diffractogram o f sample NH01-15GC3-21. Non Mineral components removed. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 81 XRD Core NH01-15 500 500 100 100 0 50 60 70 10 20 30 40 0 Two Theta Figure 30. X-ray diffractogram of sample NH01-15GC3-184. Non Mineral components removed. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Intensity 82 XRD Core NH01-15 1400 M Magnetite A Amphibole P Pyroxene Q Quartz F Feldspar (An rich) 1200 1000 800 600 F & P 400 2 0 0 0 60 50 30 40 20 10 0 Two Theta Figure 31. X-ray diffractogram of sample NFI01-15GC3-241 Non-mineral components removed. 1400 1200 1000 800 600 400 2 0 0 0 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 83 XRD El Coyote and San Juan fans 900 M Magnetite A Amphibole P Pyroxene Q Quartz F Feldspar (An rich) F & P El Coyote San Juan 0 10 20 30 40 50 60 70 80 Two Theta Figure 32. X-ray diffractogram of samples from the San Juan and El Coyote fans. A factor of 100 was added to El Coyote for graphic purposes. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 84 XRD Isla Ballena Dust Trap 600 500 400 g 300 2 0 0 100 0 Q C Calcite Q Quartz F Feldspar (An rich) H Halite P Pyroxene St Stilpnomalane 0 10 20 30 40 50 60 70 Two Theta Figure 33. X-ray diffractogram of Isla Ballena dust trap. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 600 500 400 300 2 0 0 100 0 85 eliminated because during this period, construction of a silo next to the trap’s location generated a lot of dust. Upon inspection it become obvious that the source was the soil around the construction site. Dust fluxes ranged from 0.0144 g/day/m2 to 9 9 0.031 g/day/m , averaging 0.017 g/day/m . Total flux values in Alfonso Basin 'y obtained by Silverberg (2003) ranged from 0.17 g/day/m to a maximum of 2.48 g/day/m2, averaging 0.82 g/day/m2. Considering a conservative estimate of the terrigenous contribution to be 70%, the flux of terrigenous material to the seafloor is 0.574 g/day/m2 and the eolic component is only 3% of the total sediment deposited in Alfonso Basin. Sediment trap results indicate a terrigenous contribution of 20-40 % (Silverberg, 2004. personal communication) with an eolic contribution of 5-10% of the total terrigenous sediment. Another test was done to verify the source o f the terrigenous sediment based on Rea and Hovan (1995) methodology. Sixteen selected samples from core NH01- 15GC3 were pre-treated and analyzed following their recommendations (Figure 34, Table 4). All sixteen samples had modes ca. 11 pm, very poor sorting and positive skewness suggesting a hemipelagic end member. These results are consistent with those of Bernal Franco (2001) in the adjacent La Paz Basin and Molina-Cruz et al. (2002) in Alfonso Basin. Eastern Pescadero Basin is located adjacent to the central region of the state of Sinaloa and influenced by several rivers (Figure 35) so this record should be a good indicator of precipitation. XRDs for cores NH01-26 show that the sediments for these cores are composed almost entirely o f quartz, minor an-rich feldspar and Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 86 15GC3-184cm 15GC3-241cm P a r t i c l e s i z e > f u u I5GC3-171cm 1 0 . 0 1 0 0 P a r t i c l e s i z e / j u u 15GC3-21cm ^ b . o P a r t i c l e s i z e r j i m 15GC3-18cm 15GC3-10cm ifll P a i t i c l e s i z e / j . u i i P a r t i c l e s i z e ! j u n Figure 34. Examples of results from grain size analysis for samples in where the non-mineral components were selectively removed as per Rea and Hovan (1995) proposed methodology. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 87 Table 4, Comparison of results of the grain size analysis following Rea and Hovan (1995) method to their source end-members. Sediments from Alfonso Basin are consistent with a hemipelagic source. Lower cell show an example from core NH01- 15GC3. Rea and Hovan This investigation Param eter Eolian end member Hem ipelagic end m em ber Core NHO1-15 GC3 M ode 2 pm Bim odal 2p m and 16pm -11pm Sorting M oderate M oderate to Poor Very Poor Skewness Negative Positive Positive 5 NH0M5GC3 (231cm) No Pre-Treatment 4 Non-Minera! Com ponents Removed 3 > ■ CT , 0 1 0 0 1000 0 .1 1 0 D iam eter (pm) Exam ples o f size frequency distributions for a sam ple w ith the non-m ineral com ponents rem oved and with no pre-treatm ent. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 88 LOS MOCHIS M a z a t l a n E _ C o y o t e S a n J u a n La Paz Figure 35. Gulf of California showing the location of ephimeral streams around the La Paz bay and the main rivers on the eastern margin. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 89 traces o f pyroxene and gypsum. The composition does not vary throughout the length o f the core, suggesting the same source. Baba et al. (1991) found higher quartz/feldspar ratios where upper drainages transport sediments from sedimentary, plutonic, or metamorphic rocks such as the Fuerte, Sinaloa, Piaxtla, and San Lorenzo rivers. They concluded that in the southern end of the Gulf rivers are the main contributors of terrigenous sediments. The XRD results for eastern Pescadero Basin show high quartz/feldspar ratios and thus are consistent with a fluvial source. Sediments from eastern Pescadero Basin were not treated by the Rea and Hovan (1995) methodology, however all samples from core NH01-26GC1 had very poor sorting and positive skewness, suggesting a hemipelagic origin. The lithogenic flux in the southern end of the Gulf o f California provides a proxy of fluvial/pluvial input. The terrigenous component for cores from Alfonso Basin (15 and CP) shows similar patterns. Within these cores, the relative amounts of mud vary between 70% and 90% with a very uniform average (Figure 36, Appendix E). MAR values decrease in a very consistent trend from almost 20 mg/cm2 /year in the oldest portion of the records, to about 8 mg/cm /year at core tops (Figures 37 and 38). In the center of Alfonso Basin (core 15), MAR values decrease in a step-like fashion with major changes at ca 5200, 3600, 3200, 2300, 1200 and 300 YBP. Towards the outer edge of the basin (core CP) the breaks are not as clear and they seem to decrease in a more steady fashion, however there are also some noticeable events present in this record i.e., the 6000, 4200, 3200 and 1000 YBP events. In eastern Pescadero Basin relative Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Downcore Distance (cm) 90 CALM EX NH01-15 Terrigenous Content Weight % 0 1000 50 2000 100 3000 150 4000 5000 2 0 0 6000 100 80 90 70 50 60 Figure 36. Terrigenous content weight % for CALMEX NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 91 CALMEX NH01-15 Terrigenous MAR mg/cm2 /year c ( D O u Q 0 ) V - : o o C * £ o Q 0 1000 50 2000 100 3000 150 4000 200 5000 6000 250 18 20 14 16 12 10 6 8 Figure 37. Terrigenous mass accumulation rates for CALMEX NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Distance Downcore (cm) 92 Terrigenous MAR CP mg/cm2 /year 0 1000 50 2000 3000 100 4000 5000 150 6000 7000 200 8000 14 18 20 10 12 16 6 8 Figure 38. Terrigenous Mass Accumulation Rates for core BAP96-CP, Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years Before Present 93 mud values vary mostly from 90% to 70% with one exceptional event of 57% at 8700 YBP. Prior to 7000 YBP there is considerably more variability. After 7000 YBP values center around 81% until ca 250 YBP. From 250 YBP mud decreased to current values (Figure 39). MAR values also change in step-like fashion in eastern Pescadero Basin; prior to 7200 YBP they center at about 20 mg/cm2 /year and are very variable. After 7200 YBP they decrease steadily to ca 4200 YBP and to values centered at 18 mg/cm2 /year and after a very sharp event in where it reaches 12 mg/cm2 /year the values recover and then decrease more rapidly to about 500 YBP. A 'y sharp increase occurs after this time to 18 mg/cm /year and then a drop to current values (Figures 40 and 41). The overall decrease of the terrigenous MAR indicates that the Gulf had a stronger summer monsoon mode prior to 4,200 YBP. That is to say that it had a wetter climate and has since become steadily drier, a condition that has been accentuated during the last 3000 years. This is consistent with terrestrial records in northern Mexico, Anderson and Van Devender (1995) based on pollen analysis in Sonora, found that the early Holocene was wetter and cooler than present, and warming and drying toward modem conditions in the late Holocene. Metcalfe et al. (1997) studied lake diatoms in the state o f Chihuahua, Mexico, and found similar conditions evidenced by shallowing o f lakes. Ortega Ramirez (1995) suggested that a gradual drying occurred during the early Holocene, with the driest conditions around 6000 YBP. Wetter conditions then returned and lasted until ca 3000 YBP and then a Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Distance Downcore (cm) 94 Terrigenous Sediment Content NH01-26 Weight % 0 1000 50 2000 100 3000 150 4000 200 5000 250 6000 7000 300 8000 350 9000 400 10000 85 90 55 Figure 39. Terrigenous Sediment Weight % in CALMEX NH01-26 composite core (GC1 and M CI) for eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Distance Downcore (cm) 95 Terrigenous Component MAR NH01-26 mg/cm2 /year 0 1000 50 2000 100 3000 150 4000 200 5000 250 6000 7000 300 8000 350 9000 400 10000 22 24 18 20 12 14 16 10 Figure 40. Terrigenous sediment mass accumulation rates in CALMEX NH01-26 composite core (GC1 and M CI) for eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Reproduced w ith permission o f th e copyright owner. Further reproduction prohibited without permission. Terrigenous MAR 15 10 12 14 16 18 Terrigenous MAR 26 12 14 16 18 20 22 Average ITCZ position h r > ■ ' Late period from 4,200 YBP Opal fluxes suggest constant primary productivity Increase carbonate-opal asymmetry between east and west sides Less productivity in the west Dryer and colder conditions Middle period, 7,200 to 4.200 YBP. General and steady decrease in productivity. Less variability Climatic stability. Early period ca. 10,000 to 7.200 YBP. High productivity and variability from strong north westerly winds Wetter and wanner 2000 4000 “ < fO f i ) C O “ O 6000 8000 10000 Figure 41. Terrigenous MAR records from the southern Gulf of California illustrating the climatic periods during the Holocene. The center column indicates the inferred average position of the Intertropical Convergence Zone. The right column lists the general characteristics of the period. Mass Accumulation Rates in mg/cm2 /year. so G \ 97 major drying phase began which culminated in widespread surface erosion around 2000 YBP. The step-wise decreases in MAR at 1500 and 3000 YBP correlate to the shift in summer solar insolation in the northern hemisphere and suggest stronger NW winds and reduced summer rains. Summer (May-October) insolation series were obtained using the AnalySeries software package (Paillard et al. 1996) that calculates the astronomical and daily insolation time series (the amount of solar energy received by the Earth at the top of the atmosphere) following Berger (1978) (Figures 42 and 43). The highest terrigenous MAR values occurred from 10.5 to 5.4 YBP, during the Holocene “thermal maximum”. The terrigenous input records from the southern Gulf of California are remarkably similar to those of proxies for land- derived materials obtained in the Cariaco Basin (Haug et al., 2001). The decline in terrigenous sedimentation there is interpreted as the result of the southward migration of the Intertropical Convergence Zone (ITCZ) through the Holocene (Haug et al., 2001). The position of both the Cariaco Basin and the southern Gulf relative to the ITCZ is similar and such a migration could also explain the southern G ulfs terrigenous record. As in the Cariaco Basin, the high terrigenous MAR associated with the thermal maximum would indicate a more northerly mean annual position of the ITCZ and high precipitation. An exception to the aridity trend occurred during the Little Ice Age when the Gulf experienced a considerable increase in rainfall reflected in the terrigenous input, and less intense winds reflected in the productivity proxies. This event has been Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 98 Insolation and Terrigenous MAR NH01-15 0 1000 2000 3000 4000 5000 6000 20 18 16 14 12 10 8 6 0 1000 2000 3000 4000 5000 6000 Years Before Present Figure 42. Mass accumulation rates of the terrigenous component in NH01-15 record plotted against May to October integrated insolation for latitude 24°N . Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 4 8 U 475 470 c 465 O H — O o co £ 460 455 M A R (mg/cm2 /year) 99 Insolation and Terrigenous MAR NH01-26 0 2000 4000 6000 8000 10000 24 22 20 18 16 14 12 10 0 2000 4000 6000 8000 10000 Years Before Present Figure 43. Mass accumulation rates of the terrigenous component in NH01-26 record plotted against May to October integrated insolation for latitude 24°N . Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 4yu O 465 M A R (mg/cnrf/year) 1 0 0 linked to the sunspot activity event know as the Maunder Minima (Eddy, 1976; Lean, 2002). Colder temperatures during this period allowed for northern storm systems to migrate south bringing rain. For the central Gulf, Barron et al. (2004) using geochemical proxies found a similar pattern of terrigenous sedimentation and attributed it to enhanced wintertime northwest winds. 5.2.5 Biogenic Opal Content. The biogenic opal composition in all cores analyzed is mainly diatoms and radiolaria. Values are consistently higher in eastern Pescadero than Alfonso Basin, and only very minor differences from this pattern can be observed. This east-west asymmetry suggests differences in the nutrient supply to the basins (Berger, 1973; Honjo, 1997) (Appendix F). Core BAP96-CP.- Values for CP range from a maximum of 5.94 % (50 cm) to a minimum of 0.0 % (215 cm) with an average of 4.63% and a standard deviation of 0.63 (Figure 44). Biogenic opal MAR values range from 0.0 to 1.25 mg/cm2/year, averaging 0.82 mg/cm2 /year with a standard deviation of 0.19. A drop to a value of zero occurred at 7160 YBP and after the recovery, values were centered around 1.0 mg/cm2 /year until ca. 4000 YBP, and from there, another decrease to values centered around 0.75 mg/cm2 /year until ca. 1500 YBP. Biogenic Opal dropped steadily from there to present day values of around 0.4 mg/cm2 /year (Figure 45). Core CALMEX NH01-15.- Values for 15 range from a maximum of 6.6 % (36 cm) to a minimum o f 2.4% (196 cm) with an average o f 4.7% and a standard deviation of 0.53 (Figure 46). Opal Silica MAR values range from 0.32 to Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Distance Downcore (cm) 1 0 1 CP Biogenic Opal content Weight % 0 1000 50 2000 3000 100 4000 5000 150 6000 200 7000 8000 5 6 7 2 4 3 Figure 44. Biogenic opal content weight % core BAP96-CP, Alfonso Basin, Gulf o f California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years Before Present Years Before Present 102 Biogenic Opal MAR CP mg/cm2 /year 0 1000 50 2000 3000 100 4000 150 5000 6000 200 7000 8000 0 0.2 0.4 0.6 0.8 1 1.2 1.4 Figure 45. Biogenic opal mass accumulation rates for core BAP96-CP, Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Distance Downcore (cm) Downcore Distance (cm) 103 CALMEX NH01-15 Biogenic Opal Content Weight % 0 1000 50 2000 100 3000 150 4000 5000 200 6000 3 4 5 6 7 2 Figure 46. Biogenic opal content weight % for CALMEX NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 104 7 7 1.19 mg/cm /year, averaging 0.74 mg/cm /year with a standard deviation of 0.18. Major changes on this record occurred at 26, 113 and 280 cm typified by opal maxima. Smaller changes occurred at 62 and 190 cm. A step-wise decrease of MAR values at ca. 3100 YBP, and again at ca. 2000 YBP is observed in this core (Figure 47). Core CALMEX NH01-26.- Values for 26 range from a maximum of 21.09% (331 cm) to a minimum of 8.5% (222 cm) with an average of 13.4% and a standard deviation of 1.68 (Figure 48). Opal Silica MAR values range from 5.21 to 1.88 mg/cm2/year, averaging 2.92 mg/cm2 /year with a standard deviation of 0.50. The period of 8400 to 7800 YBP is marked by a decrease in biogenic opal, and a step wise decrease of MAR values at ca. 5800 YBP, and again at ca. 4000 YBP (Figure 49). Reproducibility precision was obtained by running replicates for all cores (CP, 15 and 26). For core CP the standard deviation was 0.07 (error % = 1.5 with a standard deviation of 1.2). For core 15 the standard deviation was 0.14 (error % = 2.6, with a standard deviation o f 2.5), and for core 26 the standard deviation was 0.2 (error % = 1.6, and a standard deviation of 1.1). Bernal Franco (2001) investigated the influence of the presence o f clays on the opal content in La Paz Basin and found errors o f-3 to +0.5% with under-estimation dominating. Biogenic opal content (%) values for Alfonso Basin are less than those reported for other locations in the Gulf of California. Bernal Franco (2001) reported values between 10% and 20% for the adjacent La Paz Basin; DeMaster and Turekian Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Downcore Distance (cm) 105 CALMEX NH01-15 Biogenic Opal MAR mg/cm2/year 0 1000 50 2000 100 3000 150 4000 200 5000 6000 250 1.2 0.8 1 0.6 0.2 0.4 Figure 47. Biogenic opal mass accumulation rates for CALMEX NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Downcore Distance (cm) 106 Biogenic Opai Content in NH01-26 Weight % 2000 100 150 4000 200 250 6000 300 8000 350 400 10000 18 20 22 16 12 14 8 10 Figure 48. Biogenic Opal Content weight % in Calmex NH01-26 composite core (GC1 and M CI) for eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Distance Downcore (cm) 107 Biogenic Opal MAR in NH01-26 mg/cm2 /year 0 50 100 150 200 250 300 350 400 1.5 2 2.5 3 3.5 4 4.5 5 5.5 Figure 49. Biogenic opal content mass accumulation rates in CALMEX NH01-26 composite core (GC1 and M CI) for eastern Pescadero Basin, Gulf of California. U 2000 4000 -< CD CD C/5 00 Tl 6000 8000 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. (1987) reported a 10% to 30% range for the western margin o f the Gulf, while Thunell et al. (1994) and DeMaster and Turekian (1987) obtained values in the central basins o f 20% to 30%. For the Western margins o f the Gulf, Baba et al. (1991) reported MAR of 3.9 mg/cm2 /year, equivalent to -21% opal content. These are much higher values than those found in this investigation. The biogenic opal content in Alfonso Basin is similar to the values reported by Ganeshram and Pedersen (1988), of 4% to 11% (6-7 mg/cm2/year) for cores recovered off the coast of Mazatlan, distant from the main opal producing centers in the Gulf. The low values in Alfonso Basin cannot be explained by dilution, since terrigenous input is low when compared to other basins in the Gulf. Methodology is not a factor since all the authors used the same (i.e. Mortlock and Froelich, 1989). It follows that the export production to Alfonso Basin is low compared to the central Gulf or dissolution is higher. Low export production is to be expected for locations in the southern end of the Gulf where satellite images indicate less upwelling. Alvarez- Borrego and Lara-Lara (1991), reported that productivity in La Paz Bay is low compared to other basins in the Gulf. Molina-Cruz et al. (2002) found that a well defined thermocline exists year round in La Paz Bay which defines a steep vertical gradient of ~1°C every 4 meters, and a strong pycnocline that inhibits vertical mixing between the surface layer and the water below. This density stratification results in very low oxygen content below the pycnocline. Monreal-Gomez et al. (2001), established that the oxycline in La Paz Bay does not describe a minimum in its deeper part as it does in other regions of the Gulf, suggesting that the process of Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 109 oxidation of organic matter is less important and as a consequence primary productivity is lower. They report low chlorophyll values (0.04-0.25 m g /m ) compared to those of the central Gulf (1.5-5.0 mg/m3 ). The bathymetric sill at Boca Grande inhibits the incursion of Pacific Intermediate Water to the Bay so the exchange involves only the Equatorial Surface Water Mass, the Gulf of California Water, and the Subsurface Subtropical Water Mass (Santamaria-Del-Angel et al. 1994b; Monreal-Gomez et al. 2001; Molina-Cruz et al., 2002), and probably California Current Water. When upwelling does occur (summer-early fall), there is a dominant volume o f equatorial waters, so nutrient- poorer waters are advected to the euphotic zone creating oligotrophic conditions that do not favor diatom production. This is consistent with the work o f Santamaria-Del- Angel et al. (1994a), who found that no summer upwelling was evident in the pigment concentrations derived from coastal zone color imagery for the western Gulf of California. Sediment trap and core top samples from Alfonso Basin are filled with diatoms and silicoflagellates but they disappear downcore suggesting silica dissolution. Low biogenic silica in Alfonso basin is thus a combination of lower productivity and higher dissolution. Bernal Franco (2001) suggested that the high opal content of La Paz Basin, just outside of the La Paz Bay, may be attributed to horizontal advection from the eastern margin caused by surface geostrophic gyres described by Molina-Cruz (1988). Biogenic opal values for eastern Pescadero Basin agree with those reported Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 1 1 0 for other locations in the central-eastern Gulf of California, consistent with the general model of a eutrophic condition generated by an eastern margin dominated by upwelling (Alvarez-Borrego and Lara-Lara, 1991). Based on these results, three periods can be identified during Holocene times across the southern Gulf (Figure 50): Early Period, from ca. 10000 to 7200 YBP. This time is best represented in the record for eastern Pescadero Basin. Cores CP and CB from Alfonso Basin covered only a very small part of this period. It is characterized by high productivity and variability. Organic carbon values for this period are the highest in the record. Barron et al. (2004) found that tropical diatoms disappear from the central Gulf records during this time, and Schrader et al. (1986), for the same period and region found that species of diatoms and silicoflagellates related to cooler waters appear. The sharp opal minima at 8200 YBP (331 cm) coincide with a major global cold event described by Alley et al. (1997) and Dean et al. (2002). Barron et al. (2004) related this to increased wintertime northwest winds and deposition of biogenic silica in the central Gulf. Middle Period, from 7200 to 4200 YBP. This time is characterized by a general and steady decrease in productivity. Variability also reduces and the period appears to be one of climatic stability. Biogenic opal decreases in concert with organic carbon. Consistent with these results, Bernal Franco (2001) found for La Paz Basin that the period between 7000 and 3000 YBP was one of reduced primary productivity. An exception is noted by Barron et al. (2004), they see a major increase Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced w ith permission o f th e copyright owner. Further reproduction prohibited without permission. Biogenic Opal MAR 15 0.2 0.4 0.6 0.8 1.0 Biogenic Opal MAR 26 2 2.5 3 3.5 4 Average ITCZ position Late period from 4,200 YBP Opal fluxes suggest constant primary productivity Increase carbonate-opal asymmetry between east and west sides Less productivity in the west Dryer and colder conditions Middle period, 7,200 to 4.200 YBP. General and steady decrease in productivity. Less variability Climatic stability. Early period ca. 10,000 to 7.200 YBP. High productivity and variability from strong north westerly winds Wetter and warmer 2000 4000 - < < D fit w " 0 6000 8000 10000 Figure 50. Biogenic opal MAR records from the southern Gulf of California illustrating the climatic periods during the Holocene. The center column indicates the inferred average position of the Intertropical Convergence Zone. The right column lists the general characteristics of the period. Mass accumulation rates in mg/cm2 /year. 112 in biogenic silica in the central Gulf at 6200 YBP and suggest that it signals the persistence of summer conditions into the late fall. An event at 6300 YBP in eastern Pescadero Basin and at 6400 YBP at Alfonso Basin is evident in the southern Gulf but short lived and not as intense, perhaps because the prevailing conditions at this time in the southern Gulf were already in place and they only intensified. Late Period from 4200 YBP to the present. The beginning of this period is marked by a sharp increase in biogenic opal and a decrease until about 3000 YBP. From this time and until very late in the Holocene, eastern Pescadero Basin becomes somewhat more productive. Overall the opal fluxes suggest a period of constant primary productivity. Laminations are very well preserved suggesting low oxygen levels caused by high biological demand. This is consistent with the findings of Barron et al. (2004) for the silica-dominated central Gulf. They see that the amplitude of biogenic silica and biological productivity proxies increase at -2.4 YBP and that Octactis pulchra, a silicoflagellate indicative of high productivity in the Gulf, also increases in abundance at -2.8 YBP. Barron et al. (2004) concluded that this time was the beginning of modem oceanographic conditions with intensified ENSO cycles in the eastern Guaymas Basin. An event occurred at ca. 1400 YBP, when there is a sudden increase and then a rapid recovery across the Gulf, suggesting strong positive PDO-like mode. Following this event there is a period of reduced productivity until -1000 YBP (Medieval Warm Period), also recognized by Bemal Franco (2001) for La Paz Basin, and then two more events at ca. 800 and 300 YBP when there are sharp increases. The first one follows the Medieval Warm Period and Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 113 the last one marks the little Ice Age. In Alfonso Basin, at 3000 YBP conditions start to be different from eastern Pescadero Basin. Productivity decreases as evidenced by the decrease in biogenic opal and organic carbon. The results o f Bemal Franco (2001) for La Paz Basin for this period are consistent with those for eastern Pescadero Basin and elsewhere in the Gulf, but not with those in Alfonso Basin. 5.2.6 Total Carbon Content Total carbon % and MAR values for all cores are shown in Appendix G. Core CALMEX NH01-15. - Values range from a maximum of 8.02 % (9 cm) to a minimum of 4.63 % (203 cm) with an average of 6.5 % and a standard deviation of 0.6 (Figure 51). Total carbon MAR values range from 1.51 to 0.56 mg/cm2/year, averaging 1.0 mg/cm /year with a standard deviation of 0.2 (Figure 52). Precision was obtained with acetanilide. Standard deviation was 0.1 and % error was 0.012. Core CALMEX NH01-26. - Values range from a maximum of 5.58% (344 cm) to a minimum of 2.61% (166 cm) with an average 3.61% and a standard deviation of 0.34 (Figure 53). Total carbon MAR values range from 0.49 to 1.43 mg/cm2/year, averaging 0.78 mg/cm2 /year with a standard deviation of 0.10 (Figure 54). A run o f 13 cystine standards gave an average value o f 29.946 with a standard deviation of 0.0446 (% error = 0.001). Replicate analysis for this core resulted in an average % error of 2 .2 . Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Downcore Distance (cm) 114 CALMEX NH01-15 Total Carbon Content Weight % 0 1000 50 2000 100 3000 150 4000 5000 200 6000 4.5 5 5.5 6 6.5 7 7.5 8 8.5 Figure 51. Total carbon content for NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Downcore Distance (cm) 115 Calmex NH01-15 Total Carbon MAR mg/cm2 /year 0 1000 50 2000 100 3000 150 4000 5000 6000 250 1.4 1.6 1 1.2 0.6 0.8 0.4 Figure 52. Total carbon mass accumulation rates for NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Distance Downcore (cm) 116 Total Carbon Content in NH01-26 Weight % 2000 100 150 4000 200 250 6000 300 8000 350 400 10000 5 6 4.5 5.5 2.5 3 3.5 4 Figure 53. Total carbon content weight % in CALMEX NH01-26 composite core (GC1 and M CI) for eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 117 Total Carbon MAR in NH01-26 mg/cm2 /year 0 2000 4000 6000 8000 10000 0.4 0.6 0.8 1 1.2 1.4 1.6 Figure 54. Total carbon mass accumulation rates in CALMEX NH01-26 composite core (GC1 and M CI), eastern Pescadero Basin, Gulf of California. c C D ! — i o o £ o Q < D O u c o 0 50 100 150 200 250 300 350 400 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 118 5.2.7 Organic Carbon Content Organic carbon % and MAR values for all cores are shown in Appendix H. Core BAP96-CP.- Values range from a maximum of 8.36% (7 cm) to a minimum of 3.03% (190 cm) with an average of 5.66 % and a standard deviation of 0.93 (Figure 55) (Data from Douglas et al. 2002b). Organic carbon MAR values 9 9 range from 0.0 to 1.392 mg/cm /year, averaging 0.96 mg/cm /year with a standard deviation of 0.16 (Figure 56). Major shifts occurred at 6800, 4500 and 3000 YBP. Core CALMEX NH01-15. - Values range from a maximum of 6.85% (9 cm) to a minimum of 3.04% (200-203 cm) with an average of 4.6% and a standard deviation of 0.77 (Figure 57). Organic carbon MAR values range from 1.07 to 0.46 2 2 mg/cm /year, averaging 0.77 mg/cm”/year with a standard deviation of 0.12. Section 271-190 cm of core 15GC3 showed a uniform value of around 3.9% for organic carbon which also corresponds to a turbidite and was removed from the record (Figure 58). Core CALMEX NH01-26.- Values range from 4.26% (205 cm) to 2.52% (373 cm) with an average of 3.30 % and a standard deviation of 0.28 (Figure 59). Organic carbon MAR values range from 0.44 to 0.99 mg/cm /year, averaging 0.72 mg/cm2 /year with a standard deviation of 0.08 (Figure 60). 5.2.8 Carbonate Content In general, calcium carbonate content is higher in Alfonso Basin than eastern Pescadero Basin (Appendix I). In both locations, the carbonate is foraminifera and coccoliths (Figure 61). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Distance Downcore (cm) 119 Organic Carbon content in CP Weight % 0 1000 50 2000 3000 100 4000 150 5000 6000 200 7000 8000 250 8 9 6 7 5 3 4 Figure 55. Organic carbon content weight % for core BAP96-CP, Alfonso Basin, Gulf o f California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years Before Present Downcore Distance (cm) 120 Organic Carbon CP MAR mg/cm2/year 0 1000 50 2000 3000 100 4000 150 5000 6000 200 7000 8000 250 1 1.5 0 0.5 Figure 56. Organic carbon mass accumulation rates for core BAP96-CP, Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years Before Present Downcore Distance (cm) 121 CALMEX NH01-15 Organic Carbon Content Weight % 1000 2000 100 3000 150 4000 5000 200 6000 3 3.5 4 4.5 5 5.5 6 6.5 7 Figure 57. Organic carbon content weight % for CALMEX NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Downcore Distance (cm) 122 CALMEX NH01-15 Organic Carbon MAR mg/cm2 /year 0 1000 50 2000 100 3000 150 4000 5000 200 6000 0.4 0.5 0.6 0.7 0.8 0.9 1 1.1 Figure 58. Organic carbon mass accumulation rates for CALMEX NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Distance Downcore (cm) 123 Organic Carbon Content in NH01-26 Weight % 0 50 2000 100 150 4000 200 250 6000 300 8000 350 400 10000 4.5 4 3.5 3 2.5 Figure 59. Total organic carbon content weight % in CALMEX NH01-26 composite core (GC1 and M CI), eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 124 Organic Carbon MAR in NH01-26 mg/cm /year o Q < D O U - t — > Q 0 50 2000 100 150 4000 200 250 6000 300 8000 350 400 10000 0.9 0.8 0.6 0.7 0.5 0.4 Figure 60. Total organic carbon mass accumulation rates in CALMEX NH01-26 composite core (GC1 and M CI), eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 125 Figure 59. Scanning electron microscope (SEM) image o f a light colored lamina, core CP 164 cm. Composition is mainly coccolithophoridae debris with clay and diatom fragments. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 126 Core BAP96-CP.- Values range from a maximum o f 27.5% (107 cm) to a minimum of 1% (24 cm) with an average of 10.8% and a standard deviation of 4.9 (Figure 62). CaCCX MAR values range from 0.134 to 5.401 mg/cm /year, averaging 1.986 mg/cm2 /year with a standard deviation of 1.09. Major shifts occurred at 7200 and 3000 YBP, and smaller but significant changes at 5900, 4300, 1550, 1200 and 850 YBP (Figure 63). Core BAP94-CB. - Since subsamples for this investigation were obtained from the archive X-ray slabs and bulk density determinations were not performed when the core was recovered, carbonate content can only be presented as weight percent CaCCX. Values for CB range from a maximum o f 26.21% (106 cm) to a minimum of 4.96% (76 cm) with an average of 13.04% and a standard deviation of 4.67 (Figure 64). The larger shifts in CaCCF values coincide with values in CP at 7200 and 3000 YBP, and smaller changes at 5900 YBP, 4300 YBP, 2000 YBP, and between 550 and 1200 YBP. Core CALMEX NH01-15.- Values range from a maximum of 31.2% (146 cm) to a minimum of 4.2% (14 cm) with an average o f 14.5% and a standard deviation o f 4.5 (Figure 65). Section 271-190 cm of core 15GC3 was notable for having a uniform value of 17.5% and was identified by observation and with the aid of the X-ray records as a turbidite and removed from the record for interpretation purposes. CaCC> 3 MAR values range from 0.9 to 11.2 mg/cm2/year, averaging 4.9 mg/cm2 /year with a standard deviation of 2.4 (Figure 66). A major change on this Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Distance Downcore (cm) 127 CaCO Content in CP 3 Weight % 0 1 0 0 0 50 2 0 0 0 3000 100 4000 150 5000 6000 2 0 0 7000 8000 250 30 25 2 0 15 10 5 0 Figure 62. Carbonate content weight % in core BAP96-CP, Alfonso Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Distance Downcore (cm) 128 CaCO MAR CP 3 mg/cm2 /year 0 1000 50 2 0 0 0 3000 100 4000 5000 150 6000 7000 2 0 0 8000 6 4 5 3 1 2 0 Figure 63. Carbonate mass accumulation rates for core BAP96-CP, Alfonso Basin, Gulf o f California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years Before Present Distance Downcore (cm) 129 CaC03 Contents in CB Weight % 1 0 0 0 2 0 0 0 3000 100 4000 5000 150 6000 7000 2 0 0 8000 20 25 30 15 5 10 0 Figure 64. Carbonate content weight % in BAP96-CB core, Alfonso Basin, Gulf of California. Top 5 cm missing. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Downcore Distance (cm) 130 CALMEX NH01-15 Carbonate Content Weight % 0 1000 50 2 0 0 0 100 3000 150 4000 2 0 0 5000 6000 35 25 30 15 20 10 0 5 Figure 65. Carbonate content for NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf o f California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP Downcore Distance (cm) 131 CaCO MAR in NH01-15 3 mg/cm2 /year 0 10 0 0 50 2 0 0 0 100 3000 150 4000 5000 2 0 0 6000 6 3 4 5 0 1 2 Figure 66. Carbonate mass accumulation rates for NH01-15 composite core (GC3 and M CI), Alfonso Basin, Gulf o f California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 132 record occurred at 3000 YBP and smaller changes typified by carbonate maxima at 4800, 3800, 2600 and 800 YBP. Core CALMEX NH01-26.- Values range from an isolated maximum of 23% (345 cm; -8000 YBP) to minima of 0% (164-169 cm, 300 cm and 370 cm) with an average of 2.5 % and a standard deviation of 2.0 (Figure 67). After 8000 YBP values are very low (0-5%). CaCC> 3 MAR values range from 0.00 to 5.93 mg/cm2/year, averaging 0.57 mg/cm2 /year with a standard deviation o f 0.47, and again after 8000 YBP they are very low (0-1 mg/cm2/year) (Figure 68). Major shifts occurred at 8000, 7300 and 3000 YBP, and smaller changes at 5800, 4500, 3200, 2000, 950 and 350 YBP. Bernal Franco (2001) obtained values from 5% to 23% for three cores in La Paz Basin and they are in close agreement with those reported here for Alfonso Basin, however the trends of the series do not always agree. Starting at 3000 YBP she reports an increase in the carbonate results, while in Alfonso Basin values decrease. Trends for all other periods are in agreement. Baba et al. (1991) obtained carbonate MAR for the western slopes of the southern G ulf of 6 mg/cm2/year, higher than those for Alfonso Basin. They attributed these high values to the lower contribution of the other components in the region, creating a pattern in where the relative importance of carbonate is increased. Baba et al. (1991) also calculated carbonate MAR for various locations of the central and southern Gulf (both for the eastern and western slopes) and found that the values are fairly uniform for the entire study area. Their calculations were based on original data presented by previous Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Distance Downcore (cm) 133 CaCO Content in NH01-26 3 Weight % 2 0 0 0 100 150 4000 2 0 0 250 6000 300 8000 350 400 1 0 0 0 0 15 2 0 25 10 0 5 Figure 67. Carbonate content weight % in CALMEX NH01-26 composite core (GC1 and M CI) for eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 134 g w < D j-t O o o Q 0 > o u - 4 — » C /3 Q CaCO MAR in NH01-26 3 mg/cm2 /year 2 0 0 0 100 150 4000 2 0 0 250 6000 300 8000 350 400 1 0 0 0 0 0 Figure 68. Carbonate content mass accumulation rates in CALMEX NH01-26 composite core (GC1 and M CI) for eastern Pescadero Basin, Gulf of California. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Years BP 135 reports (van Andel, 1964; Calvert, 1966; Niemitz, 1977). Barron et al. (2004) results show that carbonate content is under 1% for almost the entire Holocene in Guaymas Basin, except for five episodes (2210, 3610, 4140, 7170 and 8310 YBP) when carbonate reached up to 2.5%. Carbonate results for eastern Pescadero Basin are consistent with those reported for the eastern slopes where biogenic opal and terrigenous sediments are dominant. Baumgartner et al. (1991b) neglected the small carbonate contribution and only considered a two-component system (opal and terrigenous sediment) in their study of the varve record in Guaymas Basin. Schrader et al. (1983) found values of less than 1% for the same region. This asymmetry is attributed to the relative contribution of the different components in accordance with the findings of Baba et al. (1991) since the actual carbonate MAR are not that different for the eastern and western slopes, nor are they for the central and southern Gulf. Carbonate content in the sediment is an imperfect proxy for productivity. However, increased productivity results in high carbon flux to the bottom and consequently high oxygen demand to degrade carbon. This results in the production of carbon dioxide and carbonic acid conducive to carbonate dissolution, so paradoxically periods of high productivity are periods o f high dissolution and thus low carbonate content. Dissolution is an important process in Alfonso Basin; Douglas et al. (2002a) found that sediments with the highest carbonate dissolution are the ones with the highest organic carbon and the lowest oxygen conditions. When carbonate values are high, organic carbon is low, however for the long-term trends of Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 136 these components they almost always agree, suggesting that long-term periods of high productivity will generate increasing long-term trends in carbonate content in the sediment record. The carbonate record in Alfonso Basin suggests three distinct periods of productivity/dissolution in the basin. The first one ends ca.7200 YBP and its difficult to characterize since the record covers only a short time, however it seem to be one of high productivity and variability. The highest values of carbonate, both percent and MAR occur during this time. A second period lasting until 4200 YBP is typified by relative stability, high variability but no change in the long-term trends. The 4200 YBP events mark the beginning of a period with very different conditions in the Gulf. Here the variability for the carbonate record increases dramatically until 3000 YBP and the trends are different for Alfonso Basin and eastern Pescadero Basin. In Alfonso Basin, there is a very important step-like decrease in carbonate followed by a steady decrease in the long-term trend, while in the eastern Pescadero Basin and in La Paz Basin (Bernal Franco, 2001) there is a step-like decrease in carbonate but it is followed by a steady increase in the long-term trend. There is an increase in the carbonate-opal asymmetry between east and west sides, with less biogenic opal in the west. The results of Bernal Franco (2001) for La Paz Basin appear to contradict this rationalization, but like the opal record, it can be attributed to horizontal advection from the eastern margin caused by surface geostrophic gyres described by Molina-Cruz (1988). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 137 5.2.9 Variability Cycles Observed. Results for the spectral analyses are shown in table 5, figures 69-75 and appendix J. Grain size parameters and terrigenous content were used to illustrate climate-related cycles. Biogenic opal content, total organic carbon and calcium carbonate content were used for productivity-related cycles. PRECIPITATION RECORDS PRODUCTIVITY RECORDS 1565 yrs (1565±55) 1633 yrs (1633+352) 829 yrs (829±44) 512 yrs (512±22) 353 yrs (353±6) 391 yrs (391±14) 252 yrs (252±10) 200 yrs (196+5) 200 yrs (198±9) 132 yrs (132±1) 140 yrs (138±7) 102 yrs (102±3) 105 yrs (105+7) 88 yrs (88±3) 90 yrs (90±3) 72 yrs (72±1) 72 yrs (72±1) 65 yrs (65±3) 52 yrs (52±2) Table 5. Summary of MTM spectra for all cores and records. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 138 1 0 ' .4 10 95% 3 10' 333 ,2 193 3 ,V.-\ 10* 257 100 ® - 4 A1 C L 10 .0 10 C arb o n ate Record Spectra C ore CB Periods in years • 1 10' - 2 10 ' 0.45 0.5 0.25 0.3 0.35 0.4 0.05 0.1 0.15 0.2 0 Frequency 10' 4 10 95 % .3 1 0 407 363 207 156 122 99 .0 1 0 ' C arb o n ate Record Spectra Core BAP96-CP Periods in years 1 0 '1 -2 10' 0.3 0.35 0.4 0.45 0.5 0.05 0.1 0.15 0.2 0.25 0 Frequency Figure 69. Power spectra calculated for carbonate records in A lfonso Basin. Top, core CB; bottom , core CP. Frequency in cycles/year. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 139 1 0 ' C arb o n ate R ecord Spectra Alfonso Basin-Gulf of California C alm ex NH01 -15GC3 a n d 15M C 11 Turbidite R em oved : Periods in years .4 10 95 % .3 1985 10; 197 794 .2 131 105 55 64 .1 a 10 .0 1 0 -1 1 0 ’ -2 1 0 ‘ 0.45 0.5 0.35 0.4 0.2 0.25 0.3 0.1 0.15 0 0.05 Frequency 10 C arb o n ate R ecord Spectra Pescadero Basin-Gulf of California C alm ex NH01-26GC1 a n d 26MC1 Periods in years .3 10 ' ,2 1 0 ‘ 804 381 180 138 261 109 1 * 5 5 10 60 54 . 0 a 10 •1 10 ' 95 % - 2 1 0 ' -3 10 ' 0.4 0.45 0.5 0.3 0.35 0.2 0.25 0.1 0.15 0 0.05 Frequency Figure 70. Power spectra calculated for the carbonate record in Alfonso and east Pescadero Basins. Top, core 15; bottom, core 26. Frequency in cycles/year. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Spectral density Spectral density 140 1 0 O rganic C arbon Record Spectra Alfonso Basin-Gulf of California C alm ex NH01-15GC3 a n d 15MC1 Turbidite Rem oved Periods in years 3 1 0 ' 95 % ,2 10' 281 1 0 484 ,o /3 3 4 1 0 242 132 56 109 - 1 1 0 ' - 2 1 0 ' -3 10 ' ,-4 1 0 ' 0.35 0.4 0.45 0.5 0.15 0.2 0.25 0.3 0 0.05 0.1 Frequency 10 O rganic C arbon MTM Record Spectra P escad ero Basin-Gulf of California C alm ex NH01-26GC1 a n d 26MC1 Periods in years .3 10' 95% > 2 10‘ 2176 .1 10 1609 407 289 192 139 10' -2 10 ' -3 10 ' -4 10' -5 10' 0.4 0.2 0.3 0.35 0.45 0.5 0 0.1 0.15 0.25 0.05 Frequency Figure 71. Power spectra calculated for the organic carbon record in Alfonso and eastern Pescadero Basins. Top, core 15; bottom, core 26. Frequency in cycles/year. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 1 0 ' Biogenic O pal Record MTM Spectra Alfonso Basin-Gulf of California C alm ex NH01 -15GC3 a n d 15MC1 Turbidite Rem oved Periods in c m years 95% 1 10 3176 625 138 321 ,o 10 107 54 58 10' -2 10 ' 0.5 0.3 0.35 0.4 0.45 0.1 0.2 0.25 0 0.05 0.15 Frequency 10' Biogenic Opal Record MTM Spectra Alfonso Basin-Gulf of California C alm ex NH01-26GC1 an d 2 6 M C l Periods in years 1510 351 169 112 1 10 49 92 .0 1 0 ' 95% •1 10' 0.35 0.45 0.5 0.3 0.4 0.05 0.1 0.15 0.2 0.25 0 Frequency Figure 72. Power spectra calculated for the biogenic opal record in Alfonso and eastern Pescadero Basins. Top, core 15; bottom, core 26. Frequency in cycles/year. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Spectral density 142 10 Terrigenous C on ten t R ecord MTM Spectra Alfonso Basin-Gulf of California C a lm ex NHO1 -15G C 3 a n d 15M C 1 Turbidite R em o v ed Periods in years 3 1 0 ' 95% 3452 201 533 ,2 1 0 ‘ 105 1 10 .0 10 0.45 0.5 0.3 0.35 0.4 0.1 0.2 0.25 0.05 0.15 0 Frequency (cycles/cm) 10 ~ i------------- r 1 0 10 1 0 10 1014 Terrigenous C o n ten t R ecord MTM S p ectra ea stern P e sc a d e r o Basin-Gulf o f California C a lm e x NH 01-26G C1 a n d 26M C1 Turbidite R e m o v e d 112 Periods in years 0 0.05 0.1 0,15 0.2 0.25 0.3 0.35 0.4 0.45 0.5 Frequency (cycles/cm) Figure 73. Power spectra calculated for the terrigenous content record in Alfonso and eastern Pescadero Basins. Top, core 15; bottom, core 26. Frequency in cycles/year. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 1 0 s M e d ia n G rain Size R e c o rd MTM S p e c tra A lfonso B asin-G ulf o f C alifornia C a lm e x N H 01-15G C 3 a n d 15M C1 Turbidite R e m o v e d P eriods in y e a rs io " 1 1 ----- : ----- 1 ----- 1 ----- “ ----- 1 ----- 1 ----- 1 ----- 1 ----- 1 ----- 1 0 0.05 0.1 0.15 0.2 0.25 D.3 0.35 0.4 0.45 0.5 Frequency . M e a n G rain Size R e c o r d ; MTM S p e c tra A lfonso B asin-G ulf o f C alifo rn ia ' C a lm e x NH01 - 15 G C 3 a n d 15M C Turbidite R e m o v e d 16 2 0 95% Periods in y e a rs 102 \A 133 A t 8 5 : V \ r ^ \ 65 l A N A 5 8 Frequency S ta n d a rd D e v ia tio n o f G rain Size R e c o rd : MTM S p e c tr a t A lfonso B asin-G ulf o f C alifo rn ia C a lm e x N H 0 1 -1 5 G C 3 a n d 15M C1 Tutbidite R e m o v e d P eriods in y e a rs 95 % 1 1557 ' V 5 3 3 • v y 3 5 9 V 1 104 „n 121 A . 88 A / \ A l 6 5 Figure 74. Power spectra calculated for grain size parameters in Alfonso Basin. Frequency in cycles/year. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 1 0 M e d ia n G rain Size R e c o rd MTM S p e c tr a P e s c a d e r o Basin-G ulf o f C alifo rn ia C a lm e x N H 01-26G C 1 a n d 2 6 M C l P erio d s in y e a rs 1 0 3 1 0 2 831 3 4 7 io ' 10° 10'2 0.15 0.2 0.25 0.3 0.35 0.4 0.45 0.5 0 0.05 0.1 Frequency 1 0 M e a n G rain Size R e c o rd MTM S p e c tr a P e s c a d e r o Basin-G ulf o f C alifo rn ia C a lm e x N H 01-26G C 1 a n d 26M C 1 Periods in y e a rs 104 1 0 3 5 74 4 97 1 0 2 10° 10-1 0.25 0.45 0.5 0 0.05 0.1 0.15 0.2 0.3 0.35 0.4 Frequency 1 0 5 S ta n d a rd D e v ia tio n o f G rain Size R e c o r d MTM S p e c tra P e s c a d e r o B asin-G ulf o f C alifo rn ia C a lm e x N H 01-26G C 1 a n d 26M C 1 P erio d s in y e a rs 1 0 4 5 1 0 103 4 9 0 351 2 6 9 102 1 0 1 10C 10' 0.15 0.2 0.25 0.3 0.35 0.4 0.45 0.5 0 0.05 0.1 Frequency Figure 75. Power spectra calculated for grain size parameters in eastern Pescadero Basin. Frequency in cycles/year. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 145 For the productivity-associated records, strong peaks o f centennial-scale variability were found with periodicities at 72 yrs (72±1), 90 yrs (90±3), 105 yrs (105±7), 140 yrs (138±7), 200 yrs (198±9), 252 yrs (252±10) and 391 yrs (391±14). All these periodicities are present prior to 3200 YBP, but the 252-year cycle dominates in the latest Holocene. Millennial-scale variations were found at 829 yrs (829±44) and 1633 yrs (1633±352) (Table 5). These cycles are associated with productivity/dissolution in the biogenic sediment record. For the precipitation associated records, significant peaks o f centennial-scale variability were found with periodicities at 52 yrs (52±2), 65 yrs (65±3), 72 yrs (72±1), 88 yrs (88±3), 102 yrs (102±3), 132 yrs (132±1), 196 yrs (196±5), 353 yrs (353±6) and 512 yrs (512±22). Millennial-scale variations were found at 1565 yrs (15651352) (Table 5). These results are in agreement with several studies (Peterson et al. 1991; Leventer et al. 1996; Campbell et al. 1998; Bernal Franco, 2001; Bond et al. 2001; Hodell et al. 2001; Poore et al., 2003) that find strong centennial-scale ocean/climate variability during the Holocene. Peterson et al. (1991), found periodicities of 381 and 200 years based on analyses of variance of G. bulloides as a proxy for upwelling intensity in the Cariaco Basin, off Venezuela. Leventer et al. (1996) obtained a 210 years cycle using marine sediment data from the Antarctic Peninsula region. Campbell et al. (1998) used grain size variations in sediments from Lake Calgary, Canada as proxies for paleoclimate and identified robust periodicities at 590, 440, Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 146 330 and 280 years. Similar productivity pulses have been identified by Bernal Franco (2001) in the biogenic record in La Paz Basin on a 330-year averaged period. Bond et al. (2001) also found periodicities within the 200-500 year range in drift-ice proxy records in the North Atlantic. A 206-year cycle has also been found in S1 8 0 and gypsum precipitation (evaporation/precipitation proxies) in the Yucatan peninsula lake records (Hodell et al. 2001), they also resolved periods of 810, 100, 50 and 39 years. Poore et al. (2003), found a significant spectral peak at near 300 years in various proxy records in the Gulf of Mexico, in addition to this peak they found others at 550, 200, 230 and 170 years. Poore et al. (2003) also analyzed runoff proxy (Ti) data from Flaug et al., (2001) and found cycles with 116 and 138-year periods. The results are also in agreement with studies that find a strong Holocene 1500±500 years rhythm (Oppo et al., 1998; Raymo et al., 1998; Campbell et al. 1998; McManus et al., 1999; Bond et al. 1997, 2001; DeMenocal et al. 2000; Viau, 2002; Poore et al. 2003). A mere coincidence in the occurrence o f similar cycles generated on a global scale by local or regional forcing is very unlikely. Thus a mechanism such as solar forcing is required that can cause changes with similar periods on a global scale. Campbell et al. (1998) suggested that the cause for the periodicity had to be external to the Earth, possibly cyclic variations in solar output. Bernal Franco (2001) suggested changes in the northern hemisphere insolation as the cause for the low frequency variability found in the Gulf of California laminated sediment record. Bond et al. (2001) were able to match the centennial scale periods to 1 0 Be and 1 4 C Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 147 nuclide production rates (solar irradiance proxies). Their interpretation of how solar variability induces a climate change implies that at times of reduced solar irradiance the atmosphere of the northern hemisphere cooled and forced a slight southward shift of the subtropical jet, and a decrease in the Northern Hadley cell circulation leading to reduced precipitation in low latitudes. Hodell et al. (2001) also related the 206-year strong cycle to nuclide production as a cause for migration o f the Hadley circulation cell and consequently of the pluvial precipitation zone in the Yucatan peninsula. Poore et al. (2003) concluded that the periodicities in their data and the 208-year cycle in 1 0 Be and 1 4 C nuclide production rates is strong evidence of the link between variations in solar output and climatic variability and that the linking mechanism is the average position of the ITCZ. Poore et al. (2003) also analyzed the I4C production rate data of Bond et al. (2001) and found significant variance at cycles of 320 [and 220 years] and linked to a 300-year cycle found in their data series from the Gulf of Mexico. Bond et al. (2001) also found a 300-year cycle in the subpolar North Atlantic records. The two most prominent cycles present in the sediments o f the southern Gulf considered in this study are the 200 year and the 140-year periods, followed by the 105 and 88-year periods. Also present are 500-year (460 and 500), 252-year, 90-year and 72-year and 65-year cycles. The 90-year could be a harmonic of the 200 and the 72 and 65-year cycles could be harmonics o f the 140-year cycle. It is clear that the main forcing for the ocean/climate variability in the southern Gulf of California is Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 148 cyclic solar output intensity and that the linking mechanism by which these changes are transferred are the variations in the relative position of the ITCZ. At the latitude of the southern Gulf, seasonal insolation variations cause expansion or contraction of the Hadley cell and migration of the relative position of the ITCZ. During the summer months when the ITCZ is close to the southern Gulf, surface winds blow from the southwest and rain is brought to the region by transferring water vapor from the equatorial region. During the wintertime, when the Hadley cell contracts and the ITCZ migrates southward, northwesterly winds shift south and intensify over the Gulf, driving upwelling. A southward migration o f the average position of the ITCZ will cause a shift to more arid conditions, less terrigenous sediment, higher productivity and more biogenic sedimentation. The centennial-scale cycles observed in the southern Gulf records are thus interpreted here as forced by the average position of the ITCZ in response to solar insolation cycles. The millennial-scale variation can be explained in the same manner by the orbital driven insolation changes over the course of the Holocene (Hodell et al. 1991; Haug et al., 2001; Poore et al. 2003). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 149 6 . CONCLUSIONS • In Alfonso Basin, average Holocene sedimentation rates at the lower basin slope are 0.27 mm/year (CP) to 0.28 mm/year (CB), while average rates in the central basin floor are 0.41 mm/year (NH015). In the eastern slope of Pescadero Basin, average rates are 0.41 mm/year. • Total MAR for core 15 before 3800 YBP, had wide amplitude but centers at 19 mg/cm2/year. After 3800 YBP, total MAR declined in a step-like fashion from 19 to 10.5 mg/cm2 /year until ca. 350 YBP. After 350 YBP there is a sharp increase to 14 mg/cm2 /year and then a decline to present values. In core 26, before 7500 YBP Total MAR centers at a value of 24 mg/cm2/year. After this time, values decline to present values but two events (4300 and 470 YBP) are evident. • In Alfonso Basin strong sediment focusing in the deepest portion of the basin is evident by the difference in thickness of correlated turbidites and average sedimentation rates across the basin. • Terrigenous sediment input in the southern Gulf o f California is predominantly of fluvial origin • Mud Flux in the southern Gulf o f California is a proxy of fluvial/pluvial input, and indicates that prior to 4200 YBP the Gulf was wetter (high rainfall) and has become steadily drier, a condition that has been accentuated during the last 3000 years. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 150 • The step-wise decreases in terrigenous MAR at 1500 and 3000 YBP correlate to the shift in summer solar insolation in the northern hemisphere and suggest stronger NW winds and reduced summer rains. • Biogenic sedimentation in the eastern side of the Gulf is opal dominant while in the western margin it is carbonate dominant. • There are 3 distinct periods of oceanographic/climatic conditions in the Gulf for the Holocene o Early period, from ca. 10000 to 7200 YBP. Characterized by high productivity and variability resulting from strong northwesterly winds and upwelling. o Middle period, from 7200 to 4200 YBP. Characterized by a general and steady decrease in productivity. Variability also reduces and the period appears to be one of climatic stability. o Late period from 4200 YBP to the present. Overall the opal flux suggests a period o f constant primary productivity, but there is an increase in the carbonate-opal asymmetry between east and west sides, with less productivity in the west. • During the Little Ice Age the Gulf experienced a considerable increase in rainfall reflected in the terrigenous input, and less intense winds reflected in the productivity proxies, an event related to a decline in sunspot activity. • Millennium scale cycles of variability occur in the southern Gulf of California at 1633, 1565, and 829 years. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 151 • Centennial scale cycles of variability occur in the southern Gulf of California at 512, 391, 353, 252, 200 and 140 years (not including possible harmonics). • Both the low and high frequency variations in sedimentation in the southern Gulf are attributed to migration of the average position o f the Intertropical Convergence Zone driven by variations in solar insolation. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 152 7. REFERENCES Alley, R.B., Mayewski, P.A., Sowers, T., Stuiver, M., Taylor, K.C., and Clark, P.U., 1997, Holocene climatic instability; a prominent, widespread event 8200 yr ago: Geology, v. 25, p. 483-486. Alvarez-Borrego, S., 1983, Gulf of California: Estuaries and enclosed seas, v. 26, p. 427-449. Alvarez-Borrego, S., and J. R. 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Sawada, 2002, Widespread evidence of 1500 yr climate variability in North America during the past 14000 yr: Geology, v. 30, p. 455-458. Zanchi, A., 1994, The opening of the Gulf of California near Loreto, Baja California, Mexico: from basin and range extension to transtensional tectonics: Journal of Structural Geology, v. 16, p. 1619-1639. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 8. APPENDICES Appendix A. Sedimentation Rates from X-Ray Grayscale in all cores. Appendix B. Grain Size Parameters for all cores (pm). Appendix C. Porosity (POR), Dry Bulk Density (DBD) and Total Mass Accumulation Rates (TMAR) in all cores. Appendix D. Summary of dust trap recovery data and flux estimates. Appendix E. Percentage and MAR of Terrigenous Sediment in all cores. Appendix F. Percentage and MAR of Biogenic Opal in all cores. Appendix G. Percentage and MAR o f Total Carbon in all cores. Appendix H. Percentage and MAR of Organic Carbon in all cores. Appendix I. Percentage and MAR o f CaC03 in all cores. Appendix J. Summary of cycles obtained with MTM Spectral Analysis in all cores. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 164 Appendix A: Sedimentation Rates fro m X-Ray Grayscale in all cores Alfonso Basin Pescadero Basin Aifonso Basin Pescadero Basin cm CP CB 15GC3 cm 26GC1 cm CP CB 15GC3 cm 26GC1 1 0.42 0.53 1 0.86 46 0.5 0.24 0.49 46 0.49 2 0.42 0.53 2 0.86 47 0.5 0.24 0.49 47 0.72 3 0.42 0.53 3 0.86 48 0.5 0.25 0.49 48 0.72 4 0.42 0.53 4 0.86 49 0.4 0.25 0.49 49 0.72 5 0.38 0.22 0.53 5 0.86 50 0.4 0.25 0.49 50 0.72 6 0.38 0.22 0.47 6 0.86 51 0.4 0.255 0.49 51 0.72 7 0.38 0.22 0.47 7 0.85 52 0.4 0.258 0.49 52 0.72 8 0.38 0.22 0.47 8 0.85 53 0.47 0.261 0.49 53 0.72 9 0.38 0.22 0.47 9 0.85 54 0.47 0.264 0.49 54 0.72 10 0.32 0.26 0.47 10 0.85 55 0.47 0.267 0.49 55 0.72 11 0.32 0.26 0.49 11 0.85 56 0.47 0.27 0.49 56 0.72 12 0.36 0.26 0.49 12 0.85 57 0.47 0.273 0.49 57 0.72 13 0.36 0.26 0.49 13 0.63 58 0.43 0.276 0.49 58 0.72 14 0.36 0.27 0.49 14 0.63 59 0.43 0.279 0.49 59 0.72 15 0.36 0.27 0.49 15 0.63 60 0.43 0.282 0.49 60 0.72 16 0.36 0.27 0.43 16 0.63 61 0.33 0.285 0.49 61 0.72 17 0.33 0.27 0.43 17 0.63 62 0.33 0.288 0.49 62 0.72 18 0.33 0.27 0.43 18 0.34 63 0.33 0.291 0.49 63 0.72 19 0.33 0.26 0.43 19 0.34 64 0.33 0.294 0.49 64 0.72 20 0.33 0.26 0.43 20 0.34 65 0.33 0.297 0.49 65 0.72 21 0.33 0.26 0.39 21 0.34 66 0.34 0.3 0.49 66 0.72 22 0.34 0.26 0.39 22 0.34 67 0.34 0.303 0.49 67 0.72 23 0.34 0.25 0.39 23 0.46 68 0.34 0.306 0.49 68 0.72 24 0.34 0.25 0.39 24 0.46 69 0.46 0.309 0.49 69 0.72 25 0.34 0.25 0.39 25 0.46 70 0.46 0.312 0.49 70 0.72 26 0.34 0.25 0.34 26 0.46 71 0.46 0.315 0.49 71 0.72 27 0.34 0.25 0.34 27 0.46 72 0.46 0.318 0.49 72 0.72 28 0.34 0.23 0.34 28 0.37 73 0.46 0.321 0.49 73 0.72 29 0.32 0.23 0.34 29 0.37 74 0.5 0.324 0.49 74 0.72 30 0.32 0.23 0.34 30 0.37 75 0.5 0.327 0.49 75 0.72 31 0.32 0.23 0.43 31 0.37 76 0.5 0.33 0.49 76 0.72 32 0.32 0.23 0.43 32 0.37 77 0.5 0.333 0.49 77 0.72 33 0.32 0.25 0.43 33 0.29 78 0.5 0.336 0.49 78 0.72 34 0.32 0.25 0.43 34 0.29 79 0.39 0.339 0.49 79 0.72 35 0.32 0.25 0.43 35 0.29 80 0.39 0.342 0.49 80 0.72 36 0.32 0.25 0.43 36 0.29 81 0.39 0.345 0.49 81 0.72 37 0.32 0.25 0.43 37 0.53 82 0.39 0.348 0.49 82 0.72 38 0.52 0.28 0.43 38 0.53 83 0.44 0.351 0.49 83 0.72 39 0.52 0.28 0.43 39 0.53 84 0.44 0.354 0.49 84 0.72 40 0.52 0.28 0.43 40 0.53 85 0.44 0.357 0.49 85 0.72 41 0.52 0.28 0.52 41 0.53 86 0.44 0.36 0.49 86 0.72 42 0.52 0.28 0.52 42 0.49 87 0.44 0.363 0.49 87 0.72 43 0.5 0.24 0.52 43 0.49 88 0.44 0.366 0.49 88 0.72 44 0.5 0.24 0.52 44 0.49 89 0.44 0.369 0.49 89 0.72 45 0.5 0,24 0.52 45 0.49 90 0.44 0.372 0.49 90 0.72 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 165 cm CP CB 15GC3 cm 26GC1 cm CP CB 15GC3 cm 26GC1 91 0.44 0.375 0.49 91 0.72 138 0.33 0.25 1.56 138 0.86 92 0.44 0.378 0.49 92 0.72 139 0.33 0.25 1.56 139 0.86 93 0.38 0.381 0.49 93 0.72 140 0.33 0.25 1.56 140 0.86 94 0.38 0.384 0.49 94 0.72 141 0.33 0.25 1.56 141 0.86 95 0.38 0.387 0.49 95 0.72 142 0.33 0.25 1.56 142 1.04 96 0.38 0.39 0.49 96 0.72 143 0.36 0.3 1.56 143 1.04 97 0.34 0.393 0.49 97 0.72 144 0.36 0.3 1.56 144 1.04 98 0.34 0.32 0.54 98 1.06 145 0.36 0.3 1.56 145 1.04 99 0.34 0.28 0.54 99 1.06 146 0.36 0.3 1.56 146 1.04 100 0.34 0.28 0.88 100 1.06 147 0.36 0.3 0.82 147 0.88 101 0.34 0.28 0.88 101 1.06 148 0.3 0.3 0.82 148 0.88 102 0.38 0.28 0.88 102 1.06 149 0.3 0.3 0.82 149 0.88 103 0.38 0.28 0.88 103 0.54 150 0.3 0.3 0.82 150 0.88 104 0.38 0.29 0.88 104 0.54 151 0.28 0.3 0.82 151 0.88 105 0.38 0.29 ? 105 0.59 152 0.28 0.3 0.7 152 1.14 106 0.38 0.29 ? 106 0.59 153 0.28 0.3 0.7 153 1.14 107 0.46 0.29 ? 107 0.59 154 0.28 0.3 0.7 154 1.14 108 0.46 0.29 ? 108 0.59 155 0.28 0.3 0.7 155 1.14 109 0.46 0.26 ? 109 0.59 156 0.28 0.3 0.7 156 1.14 110 0.46 0.26 ? 110 0.93 157 0.28 0.3 0.56 157 2.94 111 0.46 0.26 ? 111 0.93 158 0.28 0.24 0.56 158 2.94 112 0.38 0.26 ? 112 0.93 159 0.28 0.24 0.56 159 2.94 113 0.38 0.26 0.66 113 0.93 160 0.28 0.24 0.56 160 2.94 114 0.38 0.31 0.66 114 0.93 161 0.25 0.24 0.56 161 2.94 115 0.38 0.31 0.66 115 1.25 162 0.25 0.24 0.41 162 1.02 116 0.4 0.31 0.66 116 1.25 163 0.25 0.3 0.41 163 1.02 117 0.4 0.31 0.66 117 1.25 164 0.24 0.3 0.68 164 1.02 118 0.4 0.31 0.51 118 1.25 165 0.24 0.3 0.68 165 1.02 119 0.4 0.33 0.51 119 1.25 166 0.24 0.3 0.68 166 1.02 120 0.4 0.33 0.51 120 0.88 167 0.24 0.3 0.68 167 0.74 121 0.39 0.33 0.56 121 0.88 168 0.24 0.24 0.68 168 0.74 122 0.39 0.33 0.56 122 0.88 169 0.26 0.24 0.61 169 1.25 123 0.39 0.33 0.56 123 0.88 170 0.26 0.24 0.61 170 1.25 124 0.39 0.44 0.56 124 0.88 171 0.26 0.24 0.61 171 1.25 125 0.39 0.44 0.56 125 0.5 172 0.26 0.24 0.61 172 1.25 126 0.39 0.44 0.74 126 0.5 173 0.26 0.24 1.02 173 1.25 127 0.32 0.44 0.74 127 0.83 174 0.26 0.3 1.02 174 1.25 128 0.32 0.29 0.74 128 0.83 175 0.26 0.3 1.02 175 1.25 129 0.32 0.29 0.74 129 0.83 176 0.25 0.3 1.02 176 1.25 130 0.32 0.29 0.74 130 0.83 177 0.25 0.3 1.02 177 1.25 131 0.32 0.29 2 131 0.83 178 0.25 0.3 1.67 178 1.25 132 0.36 0.29 2 132 1.25 179 0.25 0.28 1.67 179 0.78 133 0.36 0.25 2 133 1.25 180 0.25 0.28 1.67 180 0.78 134 0.36 0.25 1.56 134 1.25 181 0.24 0.28 1.67 181 0.78 135 0.36 0.25 1.56 135 1.25 182 0.24 0.28 1.67 182 0.78 136 0.36 0.25 1.56 136 1.25 183 0.24 0.28 1.42 183 0.78 137 0.36 0.25 1.56 137 0.86 184 0.24 0.29 1.42 184 0.88 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 166 cm CP CB 15GC3 cm 26GC1 cm CP CB 15GC3 cm 26GC1 185 0.24 0.29 1.42 185 0.88 232 turbidite 232 0.67 186 0.23 0.29 1.42 186 0.88 233 turbidite 233 0.67 187 0.23 0.29 1.42 187 0.88 234 turbidite 234 0.67 188 0.23 0.29 0.61 188 0.88 235 turbidite 235 0.67 189 0.26 0.29 0.61 189 0.5 236 turbidite 236 0.64 190 0.26 turbidite 190 0.5 237 turbidite 237 0.64 191 0.26 turbidite 191 0.67 238 turbidite 238 0.64 192 0.26 turbidite 192 0.67 239 turbidite 239 0.64 193 0.26 turbidite 193 0.67 240 turbidite 240 0.64 194 0.25 turbidite 194 0.67 241 turbidite 241 0.65 195 0.25 turbidite 195 0,67 242 turbidite 242 0.65 196 0.25 turbidite 196 0.44 243 turbidite 243 0.65 197 0.25 turbidite 197 0.44 244 turbidite 244 0.65 198 0.25 turbidite 198 0.44 245 turbidite 245 0.65 199 0.26 turbidite 199 0.44 246 turbidite 246 0.46 200 0.24 turbidite 200 0.44 247 turbidite 247 0.46 201 0.24 turbidite 201 0.89 248 turbidite 248 0.46 202 0.24 turbidite 202 0.89 249 turbidite 249 0.46 203 0.24 turbidite 203 0.89 250 turbidite 250 0.46 204 0.24 turbidite 204 0.89 251 turbidite 251 0.45 205 0.25 turbidite 205 0.89 252 turbidite 252 0.45 206 0.25 turbidite 206 1.05 253 turbidite 253 0.45 207 0.25 turbidite 207 1.05 254 turbidite 254 0.52 208 0.25 turbidite 208 1.05 255 turbidite 255 0.52 209 0.25 turbidite 209 1.05 256 turbidite 256 0.52 210 0.22 turbidite 210 0.83 257 turbidite 257 0.52 211 turbidite 211 0.83 258 turbidite 258 0.52 212 turbidite 212 0.83 259 turbidite 259 0.64 213 turbidite 213 0.83 260 turbidite 260 0.64 214 turbidite 214 0.83 261 turbidite 261 0.64 215 turbidite 215 1.61 262 turbidite 262 0.64 216 turbidite 216 1.61 263 turbidite 263 0.64 217 turbidite 217 1.61 264 turbidite 264 0.39 218 turbidite 218 1.61 265 turbidite 265 0.39 219 turbidite 219 1.61 266 turbidite 266 0.39 220 turbidite 220 1.00 267 turbidite 267 0.39 221 turbidite 221 1.00 268 turbidite 268 0.39 222 turbidite 222 1.00 269 turbidite 269 0.41 223 turbidite 223 1.00 270 turbidite 270 0.41 224 turbidite 224 1.00 271 turbidite 271 0.41 225 turbidite 225 0.53 272 turbidite 272 0.41 226 turbidite 226 0.53 273 turbidite 273 0.41 227 turbidite 227 0.53 274 turbidite 274 0.31 228 turbidite 228 0.53 275 turbidite 275 0.85 229 turbidite 229 0.53 276 turbidite 276 0.85 230 turbidite 230 0.56 277 0.89 277 0.85 231 turbidite 231 0.67 278 0.89 278 0.85 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 167 CP CB 15GC3 cm 26GC1 cm CP CB 15GC3 cm 26GC1 279 0.89 279 0.85 326 0.71 280 0.89 280 0.83 327 0.71 281 0.89 281 0.83 328 0.71 282 0.58 282 0.83 329 0.62 283 0.58 283 0.83 330 0.62 284 0.58 284 0.83 331 0.62 285 0.58 285 0.76 332 0.62 286 0.58 286 0.76 333 0.62 287 0.56 287 0.76 334 1.14 288 0.56 288 0.76 335 1.14 289 1.14 289 0.76 336 1.14 290 1.14 290 0.82 337 1.14 291 1.14 291 0.82 338 1.14 292 1.14 292 0.82 339 0.56 293 1.14 293 0.82 340 0.56 294 1.25 294 0.82 341 0.57 295 1.25 295 0.47 342 0.57 296 1.25 296 0.47 343 0.57 297 1.25 297 0.47 344 0.57 298 1.25 298 0.69 345 0.57 299 0.92 299 0.69 346 0.46 300 0.92 300 0.69 347 0.46 301 2 301 0.69 348 0.46 302 2 302 0.69 349 0.46 303 2 303 0.83 350 0.46 304 2 304 0.83 351 0.62 305 2 305 0.83 352 0.62 306 306 0.83 353 0.62 307 307 0.83 354 0.62 308 308 0.52 355 0.62 309 0.52 356 0.43 310 0.52 357 0.43 311 0.52 358 0.43 312 0.52 359 0.43 313 0.26 360 0.66 314 0.77 361 0.66 315 0.77 362 0.66 316 0.77 363 0.66 317 0.77 364 0.66 318 0.77 365 0.56 319 0.66 366 0.56 320 0.66 367 0.56 321 0.66 368 0.56 322 0.66 369 0.56 323 0.66 370 0.52 324 0.71 371 0.52 325 0.71 372 0.52 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 168 cm CP CB 15GC3 cm 26GC1 373 0.52 374 0.52 375 1.04 376 1.04 377 1.04 378 1.04 379 1.04 380 0.79 381 0.79 382 0.79 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 169 Appendix B: Grain Size Parameters for all cores (pm) Alfonso Basin 15GC3 Turbidite removed (pm) cm Median Mean Std Dev sk 1 9.602 25.504 53.46 0.89 2 9.147 19.569 32.62 0.96 3 11.788 20.803 42.76 0.63 4 11.447 18.83 25.82 0.86 5 10.536 18.66 28.09 0.87 6 13.147 19.20 19.40 0.94 7 10.836 20.04 31.07 0.89 8 9.739 17.03 24.74 0.88 9 11.504 21.45 32.64 0.91 10 10.78 20.29 30.50 0.94 11 13.244 21.42 26.83 0.91 12 13.443 21.18 32.05 0.72 13 18.347 28.20 42.38 0.70 14 10.333 19.64 27.63 1.01 15 13.252 25.11 35.23 1.01 16 10.399 22.72 30.43 1.21 17 9.187 22.09 28.52 1.36 18 12.446 21.67 28.37 0.97 19 14.271 25.85 33.90 1.03 20 12.06 21.81 27.09 1.08 21 17.397 34.41 45.02 1.13 22 10.629 21.75 25.20 1.32 23 11.449 23.84 27.60 1.35 24 13.073 24.13 34.31 0.97 25 12.643 26.90 41.27 1.04 26 12.718 26.18 38.91 1.04 27 12.403 25.18 37.92 1.01 28 12.196 25.48 38.91 1.02 29 12.379 26.24 40.69 1.02 30 11.423 22.20 33.26 0.97 31 12.663 23.89 33.74 1.00 32 9.735 20.59 32.98 0.99 33 10.108 20.99 33.72 0.97 34 13.118 26.18 38.48 1.02 35 8.677 15.49 24.09 0.85 36 11,924 22.57 47.19 0.68 37 12.703 23.64 33.81 0.97 38 11.895 21.09 30.82 0.90 39 15.312 34.03 49.87 1.13 40 9.559 18.98 33.85 0.83 41 9.913 19.53 34.28 0.84 42 10.717 19.81 30.64 0.89 Pescadero Basin 26GC1 (pm) cm Median Mean SD Sk 1 5.00 7.68 7.70 1.04 2 6.29 9.75 10.63 0.98 3 6.04 9.34 9.97 0.99 4 7.03 10.88 11.99 0.96 5 6.31 9.61 10.14 0.98 6 6.71 10.12 10.78 0.95 7 5.75 9.73 11.41 1.05 8 5.96 10.83 13.49 1.08 9 7.34 11.48 12.93 0.96 10 6.66 10.98 12.98 1.00 11 6.75 10.31 11.12 0.96 12 5.28 14.18 29.05 0.92 13 6.40 15.79 29.73 0.95 14 5.40 12.37 19.00 1.10 15 6.11 12.96 19.96 1.03 16 7.34 14.14 19.36 1.05 17 6.34 14.63 25.85 0.96 18 6.22 14.16 25.54 0.93 19 7.31 17.71 31.89 0.98 20 6.84 14.51 20.65 1.11 21 7.68 16.85 29.72 0.92 22 6.83 16.98 32.20 0.95 23 5.85 15.52 30.52 0.95 24 5.72 13.34 24.96 0.92 25 6.15 14.35 25.40 0.97 26 7.82 16.68 27.69 0.96 27 5.66 13.64 24.97 0.96 28 5.94 13.16 22.01 0.99 29 5.86 12.68 21.09 0.97 30 5.98 12.16 20.26 0.92 31 6.25 13.55 24.13 0.91 32 7.27 13.28 21.92 0.82 33 6.86 15.91 30.05 0.90 34 5.48 13.86 25.23 1.00 35 6.91 13.86 24.08 0.87 36 7.69 15.51 24.48 0.96 37 9.19 14.77 17.12 0.98 38 9.90 17.32 21.96 1.01 39 9.25 14.11 14.94 0.98 40 8.27 13.81 15.78 1.05 41 7.78 12.88 15.33 1.00 42 7.93 12.56 14.01 0.99 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 170 43 10.257 19.22 29.27 0.92 44 13.177 25.39 36.57 1.00 45 11.734 21.61 31.64 0.94 46 9.895 19.70 31.04 0.95 47 12.446 22.36 31.26 0.95 48 11.805 18.85 24.61 0.86 49 14.375 21.75 21.99 1.01 50 12,752 21.99 30.30 0.91 51 10.494 20.16 30.78 0.94 52 8.768 17.73 29.79 0.90 53 8.083 17.11 29.02 0.93 54 11.533 18.56 20.27 1.04 55 8.618 19.00 41.94 0.74 56 11.154 17.46 18.58 1.02 57 10.889 16.60 17.49 0.98 58 10.607 20.67 31.84 0.95 59 14.379 27.11 37.61 1.02 60 9.663 19.87 32.77 0.93 61 9.391 21.53 44.40 0.82 62 8.669 19.78 42.06 0.79 63 9.474 19.20 31.46 0.93 64 10.595 21.18 33.28 0.95 65 9.909 36.07 101.85 0.77 66 10.678 18.76 26.10 0.93 67 12.006 21.78 30.39 0.97 68 9.007 15.41 22.14 0.87 69 8.588 25.33 73.30 0.68 70 12.258 20.13 24.03 0,98 71 9.829 78.36 187.69 1.10 72 11.737 113.79 223.31 1.37 73 9.558 62.07 163.70 0.96 74 8.212 23.70 70.55 0.66 75 10.196 72.02 173.73 1.07 76 13.697 139.43 237.95 1.59 77 11.793 19.35 21.59 1.05 78 11.275 21.37 31.37 0.97 79 9.273 17.26 27.49 0.87 80 10.007 20.21 41.91 0.73 81 10.192 20.68 43.16 0.73 82 11.945 20.31 26.13 0.96 83 10.918 20.40 30.26 0.94 84 12.362 25.00 46.94 0.81 85 11.305 21.66 32.08 0.97 86 12.377 22.87 32.43 0.97 87 12.802 24.35 34.13 1.01 88 11.915 26.40 50.47 0.86 89 10.942 22.51 47.86 0.73 90 9.372 18.24 28.35 0.94 43 7.50 12.33 14.29 1.02 44 8.90 14.82 28.48 0.62 45 7.38 11.32 12.18 0.97 46 6.73 12.38 23.02 0.74 47 9.22 15.19 17.17 1.04 48 9.07 15.49 17.72 1.09 49 10.99 21.72 26.44 1.22 50 10.25 15.92 16.48 1.03 51 9.13 14.71 15.87 1.06 52 8.05 16.39 20.72 1.21 53 7.28 15.07 24.35 0.96 54 8.21 17.06 28.32 0.94 55 7.55 16.24 29.11 0.90 56 6.91 15.60 26.73 0.98 57 8.66 16.31 24.78 0.93 58 6.06 14.50 27.38 0.92 59 6.32 14.69 25.31 0.99 60 6.32 15.49 27.39 1.00 61 6.74 13.57 23.42 0.87 62 7.75 18.42 32.79 0.98 63 6.94 15.13 24.81 0.99 64 7.44 20.56 34.16 1.15 65 7.03 15.85 33.17 0.80 66 6.49 13.67 21.79 0.99 67 7.59 14.72 22.06 0.97 68 8.89 15.69 23.14 0.88 69 6.96 13.97 20.79 1.01 70 7.80 15.40 24.08 0.95 71 7.86 16.50 26.46 0.98 72 6.51 14.58 25.60 0.95 73 7.67 16.49 28.93 0.91 74 7.37 17.23 31.09 0.95 75 8.25 19.52 43.55 0.78 76 7.12 15.73 38.03 0.68 77 7.14 14.49 24.64 0.90 78 5.99 13.79 24.20 0.97 79 7.07 16.46 29.42 0.96 80 6.61 13.41 22.53 0.91 81 6.57 13.44 21.73 0.95 82 7.88 14.15 19.90 0.95 83 7.57 15.33 24.49 0.95 84 7.80 17.99 27.93 1.10 85 7.55 16.28 27.23 0.96 86 5.89 12.95 23.19 0.91 87 6.08 12.75 20.94 0.96 88 4.77 10.40 16.36 1.03 89 6.13 15.41 27.74 1.00 90 5.95 13.18 20.87 1.04 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 171 91 10.144 19.44 29.90 0.93 92 18.369 37.04 49.10 1.14 93 11.931 22.03 30.95 0.98 94 10.28 18.04 33.18 0.70 95 9.989 17.56 32.45 0.70 96 12.563 22.92 31.04 1.00 97 11.112 20.51 29.24 0.96 98 11.853 20.48 26.12 0.99 99 9.295 19.44 32.07 0.95 100 9.822 20.35 46.10 0.69 101 17.073 31.24 36.10 1.18 102 14.016 24.56 29.29 1.08 103 12.279 20,68 26.71 0.94 104 14.098 24.71 31.46 1.01 105 10.187 16.97 20.35 1.00 106 11.022 21.90 33.23 0.98 107 8.616 16.23 27.16 0.84 108 9.812 17.56 25.71 0.90 109 13.705 24.54 28.26 1.15 110 10.19 20.32 31.66 0.96 111 10.946 18.93 22.77 1.05 112 10.82 19.29 24.03 1.06 113 9.735 17.58 22.33 1.05 114 11.582 21.84 30.33 1.01 115 9.594 16.19 19.16 1.03 116 8.28 18.90 42.71 0.75 117 15.99 35.84 49.68 1.20 118 10.419 21,39 33.17 0.99 119 12.164 24.10 34.70 1.03 120 10.187 20.05 31.55 0.94 121 8.682 16.18 24.78 0.91 122 8.383 16.93 26.70 0.96 123 12.741 24.89 34.23 1.06 124 16.791 38.27 53.52 1.20 125 10.741 22.53 33.00 1.07 126 10.193 19.69 27.53 1.03 127 12.193 20.99 24.77 1.07 128 12.395 20.74 23.65 1.06 129 8.186 19.21 42.03 0.79 130 10.017 19.91 30.14 0.99 131 9.526 23.17 48.24 0.85 132 7.486 13.47 17.33 1.04 133 13.784 24.08 28.08 1.10 134 10.446 19.71 25.50 1.09 135 11.498 17.93 18.69 1.03 136 20.834 40.74 50.49 1.18 137 12.074 22.66 27.88 1.14 138 9.135 14.73 17.47 0.96 91 5.94 13.43 21.39 1.05 92 6.74 14.94 25.45 0.97 93 7.00 14.02 21.56 0.98 94 6.74 12.74 18.30 0.98 95 8.68 16.64 33.27 0.72 96 7.15 12.39 16.35 0.96 97 5.50 11.17 17.16 0.99 98 6.44 12.46 17.60 1.03 99 6.06 12.11 18.09 1.00 100 4.49 8.82 12.50 1.04 101 9.54 18.70 26.15 1.05 102 7.00 15.98 27.99 0.96 103 5.54 13.09 23.42 0.97 104 6.01 11.42 16.06 1.01 105 6.48 12.20 16.79 1.02 106 7.46 13.67 19.04 0.98 107 6.89 12.45 16.54 1.01 108 7.60 13.83 19.15 0.98 109 4.66 7.72 8.53 1.07 110 6.16 11.29 15.22 1.01 111 5.64 12.23 19.44 1.02 112 6.04 10.94 14.07 1.05 113 6.13 12.21 17.80 1.02 114 5.76 14.45 25.89 1.01 115 6.15 11.42 15.87 1.00 116 6.47 11.90 16.30 1.00 117 5.32 9.85 13.17 1.03 118 6.06 10.83 13.75 1.04 119 4.53 9.25 13.61 1.04 120 4.53 9.15 13.40 1.03 121 6.11 11.17 15.56 0.97 122 5.54 10.64 14.73 1.04 123 5.08 11.21 17.94 1.03 124 6.39 13.47 19.96 1.06 125 5.46 11.79 17.95 1.06 126 6.08 11.88 16.55 1.05 127 6.19 11.29 15.07 1.02 128 4.84 9.29 12.74 1.05 129 5.16 11.24 17.30 1.05 130 5.22 15.83 8.25 3.86 131 4.35 7.88 10.07 1.05 132 6.18 13.38 23.42 0.92 133 6.03 10.70 13.62 1.03 134 6.18 11.68 15.87 1.04 135 5.69 11.57 16.95 1.04 136 6.53 11.67 15.26 1.01 137 6.27 14.25 24.78 0.97 138 5.39 11.24 21.73 0.81 Reproduced with permission of the copyright owner. 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Further reproduction prohibited without permission. 331 5.16 10.44 16.30 0.97 332 5.16 10.44 16.30 0.97 333 3.92 9.05 14.17 1.09 334 6.04 13.44 21.47 1.03 335 8.62 18.40 29.75 0.99 336 5.35 10.70 15.86 1.01 337 6.58 14.46 24.17 0.98 338 6.16 13.35 19.97 1.08 339 5.39 10.61 14.89 1.05 340 5.75 11.11 16.00 1.01 341 4.78 10,50 16.12 1.06 342 4.32 9.11 13.57 1.06 343 3.86 8.82 13.89 1.07 344 5.51 10.31 14.13 1.02 345 10.67 24.14 35.44 1.14 346 7.24 17.80 27.47 1.15 347 4.68 8.79 12.02 1.03 348 •5.87 15.23 38.73 0.72 349 5.98 17.00 40.14 0.82 350 5.55 14.66 27.70 0.99 351 5.19 12.38 21.46 1.01 352 5.60 12.63 20.46 1.03 353 4.92 9.88 14.41 1.03 354 4.10 7.73 10.15 1.07 355 4.46 9.09 13.63 1.02 356 3.64 7.78 11.66 1.06 357 4.20 8.22 11.23 1.07 358 5.45 11.20 16.33 1.05 359 3.40 6.74 8.72 1.15 360 5.40 11.52 19.35 0.95 361 6.52 14.05 23.33 0.97 362 6.09 12.61 21.72 0.90 363 5.42 12.51 21.05 1.01 364 4.89 12.14 31.60 0.69 365 3.95 12.07 33.08 0.74 366 3.79 9.91 17.60 1.04 367 5.56 14.93 26.61 1.06 368 8.90 24.21 38.57 1.19 369 6.10 19.62 35.47 1.14 370 5.56 13.84 25.57 0.97 371 3.83 10.50 18.81 1.06 372 4.26 10.82 19.58 1.01 373 4.54 12.18 23.52 0.97 374 3.85 9.88 20.03 0.90 375 5.66 14.07 24.37 1.03 376 3.87 11.88 30.59 0.79 377 3.72 9.71 19.66 0.91 378 4.92 11.41 19.18 1.02 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 177 379 4.59 12.67 24.76 0.98 380 5.12 13.53 24.92 1.01 381 4.14 9.57 16.04 1.01 382 5.67 14.08 33.83 0.75 383 4.70 13.17 35.96 0.71 384 6.13 13.73 24.26 0.94 385 5.56 16.71 33.23 1.01 386 5.66 12.82 23.57 0.91 387 4.22 8.01 10.12 1.12 388 5.32 12.49 25.34 0.85 389 5.04 11.68 21.93 0.91 390 4.72 11.57 24.10 0.85 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Appendix C: Porosity (POR), Dry Bulk Density (DBD) and Total Mass Accumulation rates (TMAR) in all cores (MAR values in mg/cm2/year) Alfonso Basin Pescadero Basin CP NH01-15 NH01-26 cm POR DBD TMAR POR DBD TMAR POR DBD TMAR 1 0.92 0.24 9.72 0.88 0.34 12.54 0.82 0.51 20.55 2 0.92 0.24 9.89 0.88 0.33 12.21 0.83 0.48 19.45 3 0.92 0.25 10.05 0.89 0.31 11.51 0.84 0.44 17.90 4 0.92 0.25 10.22 0.89 0.31 11.46 0.85 0.41 16.78 5 0.92 0.25 10.39 0.89 0.31 11.59 0.85 0.43 17.41 6 0.91 0.25 10.56 0.89 0.30 11.17 0.85 0.41 16.58 7 0.91 0.25 10.73 0.90 0.29 10.88 0.85 0.41 16.75 8 0.91 0.25 10.90 0.90 0.29 10.70 0.85 0.41 16.74 9 0.91 0.25 11.07 0.90 0.30 10.97 0.86 0.38 15.54 10 0.91 0.25 11.24 0.89 0.30 11.15 0.86 0.40 16.08 11 0.91 0.25 11.42 0.90 0.30 10.98 0.85 0.43 17.47 12 0.91 0.25 11.59 0.86 0.38 14.13 0.80 0.56 22.75 13 0.91 0.26 11.77 0.87 0.38 13.93 0.81 0.53 21.53 14 0.91 0.26 11.95 0.88 0.33 12.12 0.82 0.51 20.54 15 0.91 0.26 12.13 0.89 0.32 11.96 0.81 0.52 21.04 16 0.91 0.26 12.31 0.89 0.32 11.74 0.82 0.50 20.31 17 0.91 0.26 12.49 0.89 0.32 11.74 0.83 0.48 19.29 18 0.91 0.26 12.67 0.89 0.31 11.34 0.84 0.45 18.28 19 0.91 0.26 12.85 0.90 0.29 10.60 0.84 0.44 17.97 20 0.91 0.26 13.04 0.90 0.28 10.50 0.86 0.39 15.79 21 0.91 0.26 13.22 0.90 0.29 10.74 0.85 0.41 16.56 22 0.91 0.27 13.27 0.90 0.29 10.80 0.85 0.43 17.44 23 0.91 0.27 13.33 0.90 0.29 10.71 0.85 0.41 16.73 24 0.91 0.27 13.38 0.90 0.29 10.55 0.84 0.43 17.56 25 0.91 0.27 13.43 0.90 0.29 10.68 0.84 0.44 17.82 26 0.91 0.27 13.49 0.90 0.28 10.37 0.85 0.43 17.43 27 0.91 0.27 13.54 0.91 0.27 9.81 0.85 0.43 17.36 28 0.91 0.27 13.59 0.90 0.30 10.99 0.84 0.44 17.72 29 0.91 0.27 13.65 0.90 0.29 10.65 0.84 0.45 18.32 30 0.91 0.27 13.70 0.90 0.29 10.61 0.84 0.44 17.82 31 0.90 0.28 13.75 0.89 0.30 11.16 0.84 0.46 18.47 32 0.90 0.28 13.81 0.90 0.30 10.96 0.84 0.44 17.96 33 0.90 0.28 13.86 0.89 0.31 11.36 0.84 0.45 18.13 34 0.90 0.28 13.91 0.89 0.31 11.63 0.84 0.45 18.06 35 0.90 0.28 13.97 0.90 0.30 11.04 0.85 0.42 17.12 36 0.90 0.28 14.02 0.90 0.29 10.70 0.83 0.47 19.18 37 0.90 0.28 14.07 0.89 0.30 11.21 0.84 0.45 18.20 38 0.90 0.28 14.13 0.90 0.28 10.54 0.84 0.44 17.67 39 0.90 0.28 14.18 0.90 0.29 10.76 0.85 0.42 17.01 40 0.90 0.28 14.23 0.89 0.32 11.69 0.85 0.43 17.27 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 179 cm PO R DBD T M A R P O R DBD TMAR PO R D B D TMAR 41 0.90 0.29 14.29 0.89 0.30 11.25 0.86 0.40 16.14 42 0.90 0.29 14.34 0.90 0.29 10.72 0.83 0.47 19.14 43 0.90 0.29 14.39 0.89 0.31 11.42 0.85 0.42 16.92 44 0.90 0.29 14.45 0.89 0.31 11.41 0.84 0.46 18.43 45 0.90 0.29 14.50 0.89 0.31 11.34 0.84 0.45 18.32 46 0.90 0.29 14.55 0.90 0.30 10.97 0.84 0.44 17.74 47 0.90 0.29 14.61 0.89 0.30 11.21 0.83 0.47 19.07 48 0.90 0.29 14.66 0.90 0.29 10.84 0.82 0.49 19.95 49 0.90 0.29 14.71 0.89 0.31 11.55 0.82 0.50 20.31 50 0.90 0.30 14.77 0.90 0.30 11.00 0.82 0.50 20.04 51 0.90 0.30 14.82 0.89 0.32 11.88 0.84 0.46 18.53 52 0.90 0.30 14.87 0.88 0.33 12.39 0.83 0.46 18.76 53 0.90 0.30 14.93 0.87 0.36 13.34 0.84 0.45 18.12 54 0.90 0.30 14.98 0.88 0.33 12.32 0.83 0.48 19.60 55 0.89 0.30 15.03 0.88 0.33 12.19 0.84 0.44 17.86 56 0.89 0.30 15.09 0.87 0.36 13.28 0.82 0.50 20.24 57 0.89 0.30 15.14 0.88 0.34 12.69 0.83 0.46 18.63 58 0.89 0.30 15.19 0.89 0.32 11.78 0.84 0.43 17.54 59 0.89 0.30 15.25 0.88 0.33 12.35 0.84 0.45 18.39 60 0.89 0.31 15.30 0.88 0.35 13.06 0.83 0.48 19.25 61 0.89 0.31 15.35 0.87 0.36 13.41 0.82 0.49 19.91 62 0.89 0.31 15.41 0.87 0.36 13.40 0.81 0.51 20.68 63 0.89 0.31 15.46 0.87 0.36 13.44 0.83 0.46 18.64 64 0.89 0.31 15.51 0.88 0.35 13.06 0.83 0.47 19.02 65 0.89 0.31 15.57 0.89 0.32 11.68 0.85 0.41 16.55 66 0.89 0.31 15.62 0.88 0.33 12.14 0.85 0.43 17.43 67 0.89 0.31 15.67 0.88 0.33 12.37 0.86 0.40 16.31 68 0.89 0.31 15.73 0.88 0.35 12.78 0.83 0.48 19.40 69 0.89 0.32 15.78 0.88 0.35 12.90 0.83 0.47 19.06 70 0.89 0.32 15.83 0.88 0.33 12.35 0.83 0.47 19.18 71 0.89 0.32 15.89 0.88 0.34 12.68 0.82 0.49 19.83 72 0.89 0.32 15.94 0.87 0.35 13.13 0.82 0.50 20.40 73 0.89 0.32 15.99 0.87 0.37 13.59 0.82 0.51 20.50 74 0.89 0.32 16.05 0.88 0.33 12.38 0.83 0.48 19.29 75 0.89 0.32 16.10 0.88 0.35 12.87 0.83 0.47 19.00 76 0.89 0.32 16.15 0.88 0.35 13.01 0.83 0.48 19.38 77 0.89 0.32 16.21 0.88 0.34 12.67 0.83 0.46 18.59 78 0.89 0.33 16.26 0.87 0.37 13.82 0.83 0.47 18.83 79 0.89 0.33 16.31 0.87 q.36 13.41 0.84 0.44 17.96 80 0.88 0.33 16.37 0.88 0.35 12.96 0.85 0.42 17.06 81 0.88 0.33 16.42 0.87 0.36 13.26 0.84 0.45 18.12 82 0.88 0.33 16.47 0.88 0.34 12.73 0.85 0.41 16.58 83 0.88 0.33 16.53 0.88 0.34 12.41 0.84 0.45 18.40 84 0.88 0.33 16.58 0.87 0.36 13.37 0.83 0.48 19.36 85 0.88 0.33 16.63 0.88 0.35 12.81 0.84 0.44 17.96 86 0.88 0.33 16.69 0.87 0.37 13.68 0.84 0.45 18.28 87 0.88 0.33 16.74 0.86 0.38 14.08 0.85 0.41 16.70 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 180 cm POR DBD TMAR POR DBD TMAR POR DBD TMAR 88 0.88 0.34 16.79 0.86 0.39 14.43 0.83 0.48 19.52 89 0.88 0.34 16.85 0.87 0.38 13.93 0.84 0.43 17.57 90 0.88 0.34 16.90 0.87 0.37 13.72 0.81 0.52 21.22 91 0.88 0.34 16.95 0.90 0.28 10.28 0.83 0.48 19.32 92 0.88 0.34 17.01 0.90 0.29 10.74 0.84 0.45 18.23 93 0.88 0.34 17.06 0.86 0.39 14.38 0.83 0.48 19.37 94 0.88 0.34 17.11 0.87 0.37 13.82 0.85 0.41 16.76 95 0.88 0.34 17.17 0.86 0.40 14.91 0.84 0.45 18.03 96 0.88 0.34 17.22 0.87 0.36 13.41 0.82 0.49 19.86 97 0.88 0.35 17.27 0.87 0.37 13.51 0.82 0.49 20.03 98 0.88 0.35 17.33 0.86 0.38 14.13 0.82 0.49 19.97 99 0.88 0.35 17.38 0.86 0.40 14.71 0.81 0.52 21.12 100 0.88 0.35 17.43 0.86 0.40 14.71 0.82 0.50 20.06 101 0.88 0.35 17.49 0.86 0.39 14.44 0.83 0.47 18.91 102 0.88 0.35 17.54 0.86 0.40 14.73 0.83 0.47 18.94 103 0.88 0.35 17.59 0.86 0.39 14.26 0.81 0.53 21.52 104 0.88 0.35 17.65 0.86 0.40 14.77 0.81 0.52 21.21 105 0.87 0.35 17.70 0.86 0.38 14.20 0.82 0.49 19.70 106 0.87 0.36 17.75 0.86 0.39 14.59 0.83 0.48 19.47 107 0.87 0.36 17.81 0.85 0.42 15.47 0.82 0.49 19.96 108 0.87 0.36 17.86 0.86 0.39 14.30 0.83 0.47 19.08 109 0.87 0.36 17.91 0.86 0.38 14.19 0.83 0.46 18.67 110 0.87 0.36 17.97 0.85 0.41 15.07 0.83 0.46 18.55 111 0.87 0.36 18.02 0.86 0.39 14.45 0.83 0.47 18.95 112 0.87 0.36 18.07 0.85 0.41 15.18 0.84 0.44 17.69 113 0.87 0.36 18.13 0.86 0.39 14.48 0.83 0.46 18.55 114 0.87 0.36 18.18 0.85 0.41 15.02 0.84 0.45 18.28 115 0.87 0.36 18.23 0.86 0.39 14.43 0.83 0.47 18.95 116 0.87 0.37 18.29 0.85 0.41 15.10 0.82 0.49 19.82 117 0.87 0.37 18.34 0.86 0.41 15.00 0.80 0.55 22.10 118 0.87 0.37 18.39 0.85 0.42 15.37 0.82 0.50 20.44 119 0.87 0.37 18.45 0.86 0.39 14.43 0.81 0.51 20.80 120 0.87 0.37 18.50 0.85 0.41 15.23 0.79 0.57 22.91 121 0.87 0.37 18.55 0.85 0.43 15.81 0.81 0.53 21.26 122 0.87 0.37 18.61 0.85 0.43 15.92 0.81 0.53 21.35 123 0.87 0.37 18.66 0.86 0.40 14.75 0.82 0.50 20.12 124 0.87 0.37 18.71 0.85 0.41 18.24 0.81 0.52 20.86 125 0.87 0.38 18.77 0.85 0.42 18.52 0.82 0.49 19.69 126 0.87 0.38 18.82 0.86 0.40 17.47 0.81 0.54 21.70 127 0.87 0.38 18.87 0.86 , 0.40 17.41 0.82 0.50 20.34 128 0.87 0.38 18.93 0.86 0.39 17.06 0.82 0.51 20.60 129 0.86 0.38 18.98 0.86 0.39 17.34 0.81 0.52 21.25 130 0.86 0.38 19.03 0.86 0.39 17.16 0.80 0.54 21.81 131 0.86 0.38 19.09 0.86 0.40 17.72 0.81 0.51 20.67 132 0.86 0.38 19.14 0.85 0.41 18.02 0.82 0.50 20.05 133 0.86 0.38 19.19 0.86 0.39 17.17 0.81 0.51 20.77 134 0.86 0.38 19.25 0.86 0.39 17.20 0.83 0.48 19.45 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. cm POR DBD TMAR POR DBD TMAR POR DBD TMAR 135 0.86 0.39 19.30 0.85 0.43 18.88 0.80 0.55 22.30 136 0.86 0.39 19.35 0.85 0.42 18.63 0.81 0.52 21.04 137 0.86 0.39 19.41 0.86 0.39 17.26 0.81 0.53 21.41 138 0.86 0.39 19.46 0.85 0.41 18.06 0.80 0.55 22.21 139 0.86 0.39 19.51 0.85 0.42 18.63 0.81 0.53 21.54 140 0.86 0.39 19.57 0.84 0.43 19.03 0.81 0.51 20.67 141 0.86 0.39 19.62 0.85 0.42 18.28 0.81 0.52 21.14 142 0.86 0.39 19.67 0.85 0.42 18.52 0,81 0.53 21.58 143 0.86 0.39 19.73 0.85 0.43 18.75 0.82 0.49 19.70 144 0.86 0.40 19.78 0.86 0.40 17.81 0.82 0.49 19.65 145 0.86 0.40 19.83 0.85 0.41 18.08 0.82 0.50 20.17 146 0.86 0.40 19.89 0.85 0.42 18.43 0.83 0.48 19.50 147 0.86 0.40 19.94 0.84 0.43 19.02 0.80 0.54 21.87 148 0.86 0.40 19.99 0.84 0.44 19.32 0.81 0.52 21.05 149 0.86 0.40 20.05 0.83 0.46 20.18 0.80 0.54 21.75 150 0.86 0.40 20.10 0.82 0.50 21.95 0.80 0.54 21.84 151 0.86 0.40 20.15 0.83 0.48 20.92 0.80 0.56 22.69 152 0.86 0.40 20.21 0.83 0.46 20.33 0.79 0.59 23.81 153 0.86 0.41 20.26 0.83 0.47 20.67 0.78 0.61 24.76 154 0.85 0.41 20.31 0.83 0.48 21.27 0.79 0.58 23.34 155 0.85 0.41 20.37 0.84 0.44 19.51 0.79 0.56 22.83 156 0.85 0.41 20.42 0.85 0.43 18.83 0.80 0.56 22.60 157 0.85 0.41 20.47 0.84 0.44 19.28 0.81 0.53 21.42 158 0.85 0.41 20.53 0.84 0.44 19.28 0.79 0.58 23.56 159 0.85 0.41 20.58 0.83 0.46 20.17 0.78 0.61 24.58 160 0.85 0.41 20.63 0.83 0.46 20.18 0.78 0.60 24.22 161 0.85 0.41 20.69 0.83 0.46 20.21 0.78 0.60 24.22 162 0.85 0.41 20.74 0.83 0.46 20.26 0.78 0.59 23.87 163 0.85 0.42 20.79 0.83 0.46 20.24 0.78 0.60 24.15 164 0.85 0.42 20.85 0.84 0.45 19.93 0.78 0.59 23.98 165 0.85 0.42 20.90 0.84 0.44 19.47 0.79 0.56 22.81 166 0.85 0.42 20.95 0.85 0.42 18.33 0.77 0.63 25.36 167 0.85 0.42 21.01 0.85 0.42 18.26 0.77 0.64 25.85 168 0.85 0.42 21.06 0.85 0.42 18.46 0.78 0.60 24.10 169 0.85 0.42 21.11 0.84 0.44 19.33 0.81 0.53 21.47 170 0.85 0.42 21.17 0.85 0.41 18.04 0.83 0.47 19.03 171 0.85 0.42 21.22 0.86 0.40 17.55 0.87 0.36 14.41 172 0.85 0.43 21.27 0.86 0.40 17.50 0.87 0.36 14.69 173 0.85 0.43 21.33 0.85 0.41 17.93 0.82 0.50 20.43 174 0.85 0.43 21.38 0.85 0.42 18.51 0.79 0.56 22.81 175 0.85 0.43 21.43 0.84 0.43 19.10 0.80 0.56 22.79 176 0.85 0.43 21.49 0.86 0.40 17.62 0.80 0.55 22.28 177 0.85 0.43 21.54 0.86 0.40 17.80 0.81 0.53 21.48 178 0.84 0.43 21.59 0.85 0.43 18.74 0.81 0.52 21.05 179 0.84 0.43 21.65 0.85 0.42 18.63 0.80 0.55 22.09 180 0.84 0.43 21.70 0.84 0.44 19.49 0.79 0.57 23.25 181 0.84 0.44 21.75 0.83 0.46 20.21 0.80 0.56 22.62 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. cm POR DBD TMAR POR DBD TMAR POR DBD TMAR 182 0.84 0.44 21.81 0.85 0.43 18.94 0.80 0.55 22.42 183 0.84 0.44 21.86 0.85 0.42 18.46 0.79 0.58 23.29 184 0.84 0.44 21.91 0.85 0.42 18.26 0.79 0.57 22.90 185 0.84 0.44 21.97 0.84 0.44 19.29 0.81 0.52 21.20 186 0.84 0.44 22.02 0.85 0.42 18.52 0.80 0.56 22.60 187 0.84 0.44 22.07 0.84 0.46 20.12 0.78 0.60 24.33 188 0.84 0.44 22.13 0.85 0.43 18.72 0.79 0.58 23.37 189 0.84 0.44 22.18 0.84 0.44 19.16 0.81 0.51 20.82 190 0.84 0.44 22.23 0.84 0.44 19.40 0.79 0.56 22.84 191 0.84 0.45 22.29 0.84 0.44 19.34 0.81 0.53 21.54 192 0.84 0.45 22.34 0.83 0.46 20.28 0.80 0.55 22.09 193 0.84 0.45 22.39 0.84 0.44 19.37 0.80 0.55 22.11 194 0.84 0.45 22.45 0.84 0.44 19.53 0.80 0.56 22.65 195 0.84 0.45 22.50 0.84 0.45 19.65 0.80 0.56 22.59 196 0.84 0.45 22.55 0.85 0.43 18.74 0.81 0.53 21.36 197 0.84 0.45 22.61 0.86 0.39 17.05 0.80 0.54 21.85 198 0.84 0.45 22.66 0.84 0.44 19.39 0.81 0.52 20.94 199 0.84 0.45 22.71 0.85 0.42 18.41 0.79 0.57 23.21 200 0.84 0.46 22.77 0.83 0.46 20.39 0.80 0.55 22.29 201 0.84 0.46 22.82 0.82 0.50 21.80 0.80 0.55 22.34 202 0.84 0.46 22.87 0.80 0.56 24.53 0.79 0.58 23.59 203 0.83 0.46 22.93 0.81 0.52 22.83 0.80 0.54 21.97 204 0.83 0.46 22.98 0.81 0.54 23.59 0.80 0.54 22.02 205 0.83 0.46 23.03 0.81 0.51 22.50 0.80 0.54 21.87 206 0.83 0.46 23.09 0.82 0.49 21.62 0.79 0.58 23.31 207 0.83 0.46 23.14 0.85 0.43 18.95 0.79 0.57 23.19 208 0.83 0.46 23.19 0.85 0.43 18.81 0.79 0.57 23.25 209 0.83 0.46 23.25 0.84 0.45 19.61 0.79 0.58 23.44 210 0.83 0.47 23.30 0.84 0.45 19.74 0.79 0.58 23.28 211 0.83 0.47 23.35 0.84 0.45 19.94 0.79 0.57 22.92 212 0.83 0.47 23.41 0.84 0.45 19.82 0.79 0.57 23.01 213 0.86 0.38 16.72 0.80 0.55 22.17 214 0.86 0.40 17.50 0.81 0.52 20.92 215 0.87 0.38 16.58 0.82 0.51 20.64 216 0.84 0.46 20.09 0.81 0.54 21.67 217 0.85 0.43 18.76 0.81 0.53 21.49 218 0.83 0.46 20.29 0.81 0.53 21.34 219 0.83 0.48 21.30 0.81 0.53 21.36 220 0.82 0.48 21.31 0.81 0.51 20.82 221 0.82 0.48 21.32 0.79 0.57 23.10 222 0.82 0.49 21.70 0.80 0.54 22.03 223 0.83 0.47 20.69 0.80 0.56 22.62 224 0.83 0.46 20.18 0.81 0.53 21.49 225 0.84 0.45 19.86 0.80 0.55 22.22 226 0.84 0.45 19.75 0.79 0.58 23.43 227 0.84 0.45 19.80 0.79 0.58 23.56 228 0.84 0.45 19.77 0.78 0.60 24.31 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 183 cm POR DBD TMAR POR DBD TMAR POR DBD TMAR 229 0.85 0.43 18.89 0.79 0.58 23.37 230 0.84 0.45 19.92 0.81 0.53 21.36 231 0.84 0.45 19.86 0.80 0.56 22.53 232 0.83 0.46 20.39 0.81 0.52 21.11 233 0.84 0.44 19.18 0.82 0.50 20.37 234 0.83 0.46 20.22 0.80 0.55 22.23 235 0.84 0.46 20.04 0.80 0.55 22.12 236 0.84 0.45 19.98 0.79 0.57 23.15 237 0.84 0.45 19.80 0.79 0.58 23.53 238 0.84 0.44 19.55 0.80 0.56 22.48 239 0.79 0.58 23.32 240 0.79 0.58 23.61 241 0.78 0.61 24.50 242 0.78 0.60 24.11 243 0.78 0.60 24.31 244 0.79 0.58 23.50 245 0.80 0.55 22.46 246 0.80 0.54 21.75 247 0.80 0.56 22.68 248 0.80 0.55 22.38 249 0.81 0.53 21.65 250 0.79 0.57 23.14 251 0.79 0.58 23.63 252 0.78 0.59 23.87 253 0.78 0.60 24.13 254 0.79 0.57 23.17 255 0.80 0.56 22.77 256 0.79 0.57 23.07 257 0.79 0.59 23.79 258 0.78 0.59 23.96 259 0.80 0.56 22.49 260 0.80 0.55 22.32 261 0.79 0.59 23.84 262 0.79 0.58 23.34 263 0.80 0.55 22.34 264 0.80 0.56 22.59 265 0.79 0.58 23.64 266 0.80 0.56 22.47 267 0.79 0.57 22.98 268 0.80 0.55 22.30 269 0.80 0.56 22.50 270 0.79 0.56 22.84 271 0.79 0.57 23.07 272 0.80 0.56 22.77 273 0.79 0.56 22.83 274 0.79 0.57 22.92 275 0.79 0.57 23.10 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. cm POR DBD TMAR POR DBD TMAR POR DBD TMAR 276 0.80 0.56 22.49 277 0.80 0.56 22.47 278 0.78 0.60 24.30 279 0.79 0.57 22.87 280 0.80 0.55 22.21 281 0.80 0.55 22.38 282 0.79 0.58 23.37 283 0.79 0.56 22.80 284 0.79 0.57 22.99 285 0.78 0.60 24.10 286 0.78 0.61 24.56 287 0.78 0.61 24.67 288 0.78 0.60 24.26 289 0.79 0.56 22.83 290 0.79 0.58 23.40 291 0.78 0.60 24.20 292 0.78 0.61 24.55 293 0.78 0.61 24.83 294 0.77 0.63 25.61 295 0.78 0.60 24.21 296 0.79 0.58 23.68 297 0.79 0.58 23.56 298 0.78 0.59 24.05 299 0.78 0.59 23.90 300 0.79 0.57 23.09 301 0.78 0.60 24.15 302 0.78 0.60 24.26 303 0.77 0.62 25.13 304 0.77 0.62 25.13 305 0.76 0.66 26.66 306 0.79 0.57 23.09 307 0.80 0.55 22.40 308 0.77 0.62 25.06 309 0.76 0.65 26.11 310 0.76 0.65 26.43 311 0.77 0.64 25.80 312 0.77 0.64 25.80 313 0.80 0.54 21.88 314 0.80 0.54 21.88 315 0.79 0.58 23.28 316 0.78 0.61 24.71 317 0.77 0.63 25.45 318 0.77 0.63 25.35 319 0.77 0.62 24.99 320 0.79 0.58 23.68 321 0.78 0.61 24.78 322 0.78 0.61 24.58 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. cm POR DBD TMAR POR DBD TMAR POR DBD TMAR 323 0.77 0.64 25.77 324 0.77 0.63 25.57 325 0.77 0.64 25.96 326 0.77 0.63 25.46 327 0.76 0.65 26.19 328 0.77 0.62 25.22 329 0.78 0.60 24.25 330 0.80 0.55 22.17 331 0.81 0.52 21.05 332 0.81 0.53 21.44 333 0.79 0.58 23.32 334 0.77 0.62 24.94 335 0.77 0.62 25.15 336 0.78 0.59 24.05 337 0.79 0.59 23.79 338 0.78 0.61 24.78 339 0.77 0.63 25.46 340 0.77 0.62 25.21 341 0.78 0.61 24.52 342 0.77 0.62 25.22 343 0.77 0.62 25.11 344 0.77 0.63 25.37 345 0.77 0.64 25.72 346 0.77 0.62 25.02 347 0.78 0.61 24.52 348 0.80 0.54 21.80 349 0.81 0.54 21.68 350 0.80 0.54 22.02 351 0.79 0.58 23.57 352 0.77 0.63 25.37 353 0.79 0.59 23.72 354 0.80 0.54 21.91 355 0.80 0.54 21.81 356 0.80 0.54 22.04 357 0.78 0.59 24.05 358 0.78 0.60 24.32 359 0.79 0.59 23.85 360 0.79 0.59 23.78 361 0.78 0.59 23.93 362 0.78 0.60 24.38 363 0.80 0.56 22.66 364 0.80 0.55 22.25 365 0.81 0.54 21.66 366 0.79 0.57 22.98 367 0.78 0.61 24.55 368 0.80 0.55 22.44 369 0.79 0.58 23.31 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 186 POR DBD TMAR POR DBD TMAR POR DBD TMAR 370 371 372 373 374 375 376 377 378 379 380 381 382 383 384 385 386 387 388 389 390 0.79 0.57 23.22 0.79 0.58 23.46 0.78 0.60 24.36 0.78 0.59 24.04 0.78 0.60 24.48 0.77 0.62 25.11 0.77 0.62 25.10 0.77 0.62 25.25 0.77 0.63 25.67 0.77 0.64 25.96 0.77 0.62 25.29 0.77 0.63 25.54 0.77 0.62 25.19 0.77 0.63 25.37 0.76 0.64 26.00 0.76 0.65 26.47 0.76 0.65 26.15 0.76 0.65 26.50 0.76 0.64 26.10 0.77 0.63 25.41 0.77 0.64 25.78 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. cm POR DBD TMAR POR DBD TMAR POR DBD TMAR 370 371 372 373 374 375 376 377 378 379 380 381 382 383 384 385 386 387 388 389 390 0.79 0.57 23.22 0.79 0.58 23.46 0.78 0.60 24.36 0.78 0.59 24.04 0.78 0.60 24.48 0.77 0.62 25.11 0.77 0.62 25.10 0.77 0.62 25.25 0.77 0.63 25.67 0.77 0.64 25.96 0.77 0.62 25.29 0.77 0.63 25.54 0.77 0.62 25.19 0.77 0.63 25.37 0.76 0.64 26.00 0.76 0.65 26.47 0.76 0.65 26.15 0.76 0.65 26.50 0.76 0.64 26.10 0.77 0.63 25.41 0.77 0.64 25.78 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 188 Appendix D Summary of dust trap recovery data and flux estimates Date Period Days out Trap area 0.0491 4/6/2002 set up 0 8/8/2002 I 123 1/8/2003 II 153 5/8/2003 III 118 8/12/2003 IV 95 Trap 1 Trap 2 Trap 3 Trap 4 Trap 5 El Coyote Las Animas Microondas Pichilingue Bailena Island Sample weight in grams after organic debris removed set up set up set up set up set up I 0.089 0 0.092 0.087 0.146 II 0.147 0.093 0.112 0.912 0.186 III 0 0 0 0 0.101 IV 0 0 0 0 0 Sample weight/ day I 0.000723577 0 0.000747967 0.000707317 0.001186992 II 0.001195122 0.000756098 0.000910569 0.007414634 0.001512195 III 0 0 0 0 0.000821138 IV 0 0 0 0 0 Estimated Dust Flux (g/day/m2) I 0.01474056 0 0.015237433 0.014409311 0.024 II 0.024346768 0.015403057 0.018549918 0.151049333 0.031 III 0 0 0 0 0.017 IV 0 0 0 0 0 Silverberg's et al. 2003 Total Flux values min 0.17 g/day/m2 max 2.48 aver 0.82 Average Dust flux for ail traps excluding no recovery periods is 0.017g/day/m2 Assuming a 70% terrigenous component for Alfonso Basin Flux=0.574 g/day/m2 Dust flux represents 3% of total flux to the bottom. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 189 Appendix E: Percentage and MAR of Terrigenous Sediment in all cores (MAR values in mg/cm2/year) Alfonso Basin CP NH01-15 Pescadero Basin NH01-26 Alfonso Basin CP NH01-15 Pescadero Basin NH01-26 cm % MAR % MAR cm % MAR cm % MAR % MAR cm % MAR 1 78.66 7.65 74.62 9.36 1 75.47 15.51 42 80.43 11.53 79.96 8.57 42 80.80 15.46 2 80.02 7.91 78.48 9.58 2 75.69 14.72 43 84.63 12.18 79.80 9.12 43 79.57 13.46 3 82.25 8.27 80.12 9.22 3 75.89 13.59 44 78.97 11.41 77.65 8.86 44 79.53 14.66 4 82.97 8.48 82.05 9.40 4 75.76 12.71 45 82.65 11.98 76.45 8.67 45 80.03 14.67 5 80.64 8.38 82.70 9.58 5 76.92 13.39 46 85.01 12.37 78.28 8.59 46 79.80 14.16 6 85.02 8.98 82.17 9.18 6 78.82 13.07 47 83.02 12.13 79.78 8.95 47 78.13 14.90 7 85.15 9.13 78.95 8.59 7 77.06 12.91 48 85.80 12.58 79.83 8.65 48 79.62 15.88 8 81.93 8.93 78.67 8.42 8 78.02 13.06 49 86.40 12.71 78.61 9.08 49 79.86 16.22 9 81.47 9.02 78.34 8.59 9 76.54 11.90 50 87.93 12.98 77.47 8.52 50 79.26 15.88 10 78.33 8.81 79.86 8.90 10 76.65 12.33 51 88.05 13.05 77.77 9.24 51 79.80 14.79 11 80.42 9.18 80.77 8.87 11 76.42 13.35 52 86.29 12.84 78.61 9.74 52 76.98 14.44 12 79.79 9.25 83.75 11.84 12 77.86 17.72 53 84.55 12.62 79.42 10.60 53 79.16 14.34 13 82.48 9.71 83.95 11.69 13 78.51 16.90 54 83.86 12.56 79.07 9.74 54 79.50 15.58 14 80.16 9.58 84.76 10.27 14 78.37 16.10 55 85.57 12.86 77.94 9.50 55 78.77 14.06 15 80.26 9.73 81.75 9.77 15 78.79 16.57 56 82.93 12.51 77.56 10.30 56 79.31 16.05 16 77.80 9.57 81.62 9.58 16 77.99 15.84 57 81.39 12.32 79.75 10.12 57 77.43 14.43 17 79.30 9.90 77.46 9.09 17 77.64 14.97 58 82.23 12.49 80.61 9.50 58 80.37 14.10 18 81.28 10.30 78.17 8.86 18 79.91 14.61 59 81.28 12.39 77.05 9.51 59 81.97 15.08 19 79.39 10.20 79.51 8.43 19 78.08 14.03 60 80.09 12.25 78.88 10.30 60 81.64 15.72 20 80.08 10.44 78.19 8.21 20 77.77 12.28 61 82.02 12.59 75.69 10.15 61 82.04 16.34 21 78.73 10.41 78.58 8.44 21 80.11 13.26 62 81.96 12.63 78.85 10.57 62 81.67 16.89 22 73.74 9.79 77.55 8.37 22 79.09 13.79 63 88.25 13.64 76.67 10.30 63 81.28 15.15 23 83.80 11.17 77.86 8.34 23 80.51 13.47 64 83.48 12.95 80.03 10.45 64 79.35 15.10 24 88.31 11.82 78.26 8.25 24 79.99 14.05 65 83.12 12.94 77.07 9.00 65 80.43 13.31 25 86.53 11.62 78.22 8.35 25 78.89 14.06 66 82.15 12.83 78.82 9.57 66 81.20 14.15 26 87.92 11.86 78.43 8.13 26 77.94 13.58 67 82.69 12.96 80.13 9.91 67 80.49 13.13 27 83.64 11.33 77.14 7.57 27 79.28 13.76 68 79.94 12.57 82.51 10.55 68 81.90 15.89 28 87.37 11.88 78.85 8.66 28 79.14 14.02 69 77.79 12.28 84.13 10.85 69 78.84 15.02 29 83.80 11.44 77.50 8.25 29 80.17 14.69 70 80.99 12.82 83.34 10.29 70 80.89 15.52 30 80.23 10.99 76.50 8.12 30 78.84 14.05 71 75.33 11.97 82.83 10.51 71 79.56 15.78 31 82.66 11.37 78.45 8.75 31 78.96 14.59 72 83.23 13.27 81.95 10.76 72 79.04 16.13 32 83.57 11.54 78.04 8.55 32 77.68 13.95 73 85.05 13.60 80.60 10.95 73 79.39 16.27 33 83.69 11.60 75.13 8.53 33 77.70 14.09 74 87.18 13.99 82.62 10.23 74 80.02 15.44 34 81.89 11.39 79.25 9.22 34 80.16 14.48 75 83.97 13.52 80.76 10.39 75 79.50 15.11 35 80.52 11.25 80.58 8.89 35 80.30 13.75 76 79.73 12.88 78.67 10.24 76 79.66 15.44 36 77.91 10.92 78.07 8.35 36 79.55 15.26 77 74.14 12.02 80.34 10.17 77 80.25 14.92 37 79.62 11.21 77.96 8.74 37 80.12 14.58 78 81.00 13.17 78.39 10.83 78 80.71 15.20 38 80.66 11.39 79.33 8.36 38 78.90 13.95 79 84.04 13.71 78.99 10.59 79 81.08 14.56 39 77.90 11.05 74.34 8.00 39 79.80 13.57 80 85.48 13.99 80.42 10.43 80 80.59 13.75 40 78.00 11.10 72.16 8.44 40 80.08 13.83 81 86.24 14.16 78.89 10.46 81 82.62 14.97 41 79.09 11.30 76.03 8.56 41 79.85 12.89 82 82.99 13.67 80.63 10.27 82 82.28 13.64 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 190 cm % MAR % MAR cm % MAR 83 83.15 13.74 77.79 9.65 83 82.54 15.19 84 80.31 13.32 81.67 10.92 84 80.37 15.56 85 79.12 13.16 76.75 9.83 85 82.88 14.88 86 79.65 13.29 76.75 10.50 86 83.53 15.27 87 77.04 12.90 81.94 11.54 87 82.98 13.86 88 81.40 13.67 83.02 11.98 88 82.67 16.14 89 83.71 14.10 80.40 11.20 89 80.72 14.19 90 79.16 13.38 82.39 11.31 90 81.76 17.35 91 82.98 14.07 82.09 8.44 91 81.49 15.75 92 86.34 14.68 74.76 8.03 92 81.71 14.90 93 85.00 14.50 77.91 11.20 93 81.27 15.74 94 79.80 13.66 83.70 11.57 94 82.14 13.77 95 80.49 13.82 78.22 11.66 95 81.21 14.64 96 81.23 13.99 77.87 10.44 96 80.06 15.90 97 76.01 13.13 76.23 10.30 97 82.30 16.48 98 72.88 12.63 72.15 10.20 98 81.62 16.30 99 67.22 11.68 74.43 10.95 99 81.04 17.11 100 73.36 12.79 81.30 11.96 100 82.88 16.63 101 79.40 13.88 80.64 11.64 101 83.67 15.82 102 78.47 13.76 79.71 11.74 102 82.19 15.57 103 79.97 14.07 79.92 11.40 103 80.82 17.39 104 75.99 13.41 80.73 11.92 104 80.10 16.99 105 73.16 12.95 80.45 11.42 105 81.48 16.06 106 77.81 13.81 77.04 11.24 106 81.65 15.90 107 63.18 11.25 78.25 12.10 107 81.33 16.23 108 73.07 13.05 80.72 11.54 108 80.42 15.35 109 74.31 13.31 79.59 11.29 109 80.84 15.09 110 71.94 12.93 78.11 11.77 110 80.34 14.91 111 65.63 11.83 76.84 11.10 111 78.92 14.96 112 69.05 12.48 78.09 11.85 112 81.59 14.43 113 76.34 13.84 75.49 10.93 113 79.79 14.80 114 74.92 13.62 78.54 11.79 114 80.68 14.75 115 67.54 12.32 78.22 11.28 115 81.08 15.37 116 71.54 13.08 78.51 11.85 116 80.02 15.86 117 73.70 13.52 72.63 10.89 117 81.40 17.99 118 78.81 14.50 73.15 11.24 118 83.66 17.10 119 78.27 14.44 79.73 11.50 119 82.32 17.12 120 68.90 12.75 74.08 11.28 120 81.81 18.74 121 71.79 13.32 73.10 11.56 121 79.99 17.00 122 76.01 14.14 71.32 11.36 122 80.28 17.14 123 73.19 13.66 63.78 9.41 123 78.52 15.80 124 75.90 14.20 63.40 11.56 124 80.41 16.77 125 76.78 14.41 65.89 12.20 125 80.98 15.95 126 81.74 15.38 71.73 12.53 126 82.30 17.86 127 74.50 14.06 80.99 14.10 127 79.79 16.23 128 75.96 14.38 79.26 13.52 128 82.37 16.97 129 74.64 14.17 79.17 13.73 129 81.70 17.36 % MAR % MAR cm % MAR 77.40 14.73 78.50 13.47 130 80.94 17.66 73.69 14.07 77.42 13.72 131 84.60 17.49 79.30 15.18 77.31 13.93 132 81.01 16.24 79.45 15.25 79.00 13.56 133 80.75 16.77 77.82 14.98 76.52 13.16 134 81.51 15.85 80.84 15.60 73.21 13.82 135 81.11 18.09 83.21 16.10 75.74 14.11 136 82.01 17.25 79.89 15.51 70.26 12.13 137 80.61 17.26 75.56 14.70 69.09 12.48 138 78.61 17.45 76.91 15.01 67.40 12.55 139 77.84 16.77 76.37 14.94 71.62 13.63 140 78.69 16.27 76.95 15.10 77.32 14.14 141 78.24 16.54 81.91 16.11 80.67 14.94 142 78.86 17.02 80.45 15.87 75.64 14.18 143 79.63 15.69 77.27 15.28 63.24 11.26 144 82.65 16.24 78.03 15.48 62.15 11.24 145 80.70 16.28 81.78 16.26 61.60 11.35 146 80.96 15.78 79.64 15.88 70.38 13.39 147 82.89 18.13 77.64 15.52 70.06 13.53 148 81.49 17.15 81.55 16.35 72.85 14.70 149 80.55 17.52 80.64 16.21 77.94 17.11 150 82.11 17.93 79.01 15.92 80.71 16.89 151 78.98 17.92 83.20 16.81 73.40 14.92 152 80.76 19.23 83.16 16.85 66.93 13.83 153 80.96 20.04 83.24 16.91 69.82 14.85 154 80.10 18.70 79.98 16.29 71.27 13.90 155 81.04 18.50 78.28 15.99 70.88 13.35 156 80.99 18.30 81.09 16.60 74.48 14.36 157 79.74 17.08 82.81 17.00 76.29 14.71 158 78.11 18.40 77.35 15.92 79.05 15.95 159 79.41 19.52 80.34 16.58 79.36 16.02 160 77.68 18.82 79.39 16.42 73.31 14.81 161 80.54 19.51 78.65 16.31 70.33 14.25 162 80.18 19.14 74.58 15.51 71.75 14.52 163 82.42 19.91 79.06 16.48 72.30 14.41 164 84.72 20.32 81.08 16.95 71.97 14.01 165 82.17 18.75 84.52 17.71 72.39 13.27 166 81.25 20.60 84.27 17.70 78.25 14.29 167 81.34 21.03 79.35 16.71 79.92 14.75 168 78.40 18.90 72.67 15.34 78.00 15.08 169 79.00 16.96 79.90 16.91 79.08 14.26 170 80.38 15.30 79.40 16.85 76.90 13.50 171 79.52 11.46 75.64 16.09 77.33 13.53 172 81.09 11.91 78.43 16.73 78.77 14.12 173 82.42 16.83 80.36 17.18 73.76 13.65 174 83.25 18.99 77.86 16.69 74.25 14.18 175 82.06 18.70 80.02 17.19 79.03 13.93 176 83.58 18.62 cm 130 131 132 133 134 135 136 137 138 139 140 141 142 143 144 145 146 147 148 149 150 151 152 153 154 155 156 157 158 159 160 161 162 163 164 165 166 167 168 169 170 171 172 173 174 175 176 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 191 cm % MAR % MAR cm % MAR cm % MAR % MAR cm % MAR 177 83.53 17.99 70.28 12.51 177 83.43 17.92 224 76.45 15.43 224 82.52 17.74 178 83.49 18.03 72.26 13.54 178 83.25 17.52 225 77.89 15.47 225 81.80 18.17 179 87.19 18.87 72.51 13.51 179 82.67 18.26 226 77.88 15.38 226 81.20 19.02 180 81.12 17.60 72.13 14.06 180 83.26 19.35 227 80.46 15.93 227 82.28 19.38 181 81.19 17.66 75.69 15.29 181 83.63 18.92 228 76.01 15.03 228 82.19 19.98 182 78.56 17.13 78.04 14.78 182 82.80 18.56 229 71.45 13.50 229 80.25 18.75 183 80.64 17.63 80.11 14.79 183 82.28 19.16 230 74.50 14.84 230 81.43 17.40 184 80.10 17.55 76.87 14.04 184 84.30 19.30 231 77.96 15,48 231 78.81 17.75 185 79.02 17.36 79.32 15.30 185 82.39 17.47 232 78.96 16.10 232 79.13 16.70 186 82.37 18.14 72.56 13.44 186 82.02 18.53 233 75.09 14.40 233 80.91 16.48 187 82.35 18.18 70.90 14.27 187 82.38 20.05 234 75.74 15.31 234 82.11 18.25 188 83.84 18.55 78.95 14.78 188 81.16 18.96 235 77.99 15.63 235 81.05 17.93 189 84.42 18.73 77.55 14.86 189 80.76 16.82 236 79.43 15.87 236 79.95 18.51 190 83.33 18.53 68.47 13.28 190 79.67 18.19 237 73.30 14.51 237 78.97 18.58 191 75.03 16.72 76.51 14.80 191 80.85 17.42 238 77.10 15.07 238 80.72 18.15 192 76.07 16.99 80.02 16.23 192 82.68 18.26 239 81.32 18.96 193 82.06 18.38 74.88 14.50 193 81.60 18.04 240 80.29 18.95 194 80.17 18.00 75.74 14.80 194 82.70 18.73 241 79.99 19.60 195 83.12 18.70 68.79 13.52 195 80.86 18.26 242 80.41 19.39 196 79.17 17.86 81.59 15.29 196 82.50 17.63 243 81.32 19.77 197 80.89 18.29 80.06 13.65 197 82.98 18.13 244 78.54 18.46 198 78.16 17.71 81.20 15.74 198 82.10 17.19 245 78.30 17.58 199 81.20 18.44 73.01 13.44 199 80.99 18.80 246 79.46 17.29 200 86.27 19.64 75.82 15.46 200 78.05 17.40 247 77.89 17.67 201 78.73 17.97 76.65 16.71 201 80.92 18.07 248 78.84 17.65 202 69.37 15.87 77.99 19.13 202 82.03 19.35 249 79.46 17.20 203 72.64 16.66 77.87 17.78 203 82.08 18.03 250 78.77 18.22 204 68.97 15.85 78.80 18.59 204 83.20 18.32 251 78.08 18.45 205 74.41 17.14 78.31 17.62 205 75.48 16.51 252 79.51 18.98 206 74.98 17.31 74.50 16.10 206 81.66 19.03 253 79.30 19.13 207 73.69 17.05 78.49 14.87 207 83.38 19.33 254 80.66 18.69 208 74.94 17.38 83.72 15.74 208 81.08 18.85 255 78.03 17.76 209 69.37 16.13 83.08 16.29 209 82.04 19.23 256 81.56 18.81 210 73.18 17.05 81.13 16.01 210 84.28 19.62 257 76.40 18.17 211 75.81 17.71 80.11 15.98 211 84.24 19.31 258 81.76 19.59 212 81.44 19.06 77.57 15.38 212 82.56 18.99 259 77.61 17.45 213 75.89 12.69 213 78.20 17.34 260 80.38 17.94 214 81.93 14.33 214 81.27 17.00 261 80.80 19.26 215 80.63 13.37 215 81.98 16.92 262 81.30 18.98 216 79.42 15.95 216 83.88 18.18 263 78.97 17.64 217 81.67 15.32 217 83.71 17.99 264 78.13 17.65 218 76.72 15.57 218 81.86 17.47 265 79.59 18.82 219 74.44 15.85 219 83.83 17.91 266 78.88 17.72 220 75.38 16.07 220 84,12 17.52 267 77.94 17.91 221 77.78 16.58 221 83.84 19.37 268 75.90 16.93 222 77.69 16.86 222 85.68 18.87 269 79.39 17.86 223 77.11 15.95 223 82.28 18.61 270 79.03 18.05 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 192 MAR % MAR cm % MAR 271 78.98 18.22 272 79.17 18.02 273 81.00 18.49 274 81.81 18.75 275 79.95 18.47 276 80.00 17.99 277 79.76 17.92 278 79.92 19.42 279 81.36 18.61 280 80.84 17.95 281 79.83 17.87 282 82.66 19.31 283 82.24 18.75 284 83.06 19.10 285 80.98 19.52 286 81.71 20.07 287 74.49 18.38 288 80.14 19.44 289 81.53 18.61 290 81.75 19.13 291 79.59 19.26 292 80.88 19.86 293 84.38 20.95 294 83.71 21.43 295 81.01 19.61 296 80.60 19.09 297 80.13 18.88 298 80.35 19.33 299 80.73 19.29 300 82.33 19.01 301 80.92 19.54 302 80.04 19.42 303 80.12 20.13 304 80.63 20.26 305 84.03 22.40 306 82.66 19.09 307 81.96 18.36 308 81.83 20.51 309 80.43 21.00 310 80.34 21.24 311 81.14 20.94 312 81.24 20.96 313 80.19 17.55 314 79.04 17.30 315 79.98 18.62 316 71.49 17.67 317 76.76 19.53 cm % MAR % MAR cm % MAR 318 80.83 20.49 319 78.13 19.53 320 79.83 18.90 321 81.97 20.32 322 80.43 19.77 323 80.65 20.78 324 85.37 21.83 325 84.74 22.00 326 83.71 21.31 327 83.17 21.78 328 82.65 20.85 329 82.40 19.98 330 80.89 17.93 331 73.20 15.41 332 79.64 17.07 333 84.96 19.81 334 85.52 21.33 335 80.55 20.26 336 74.85 18.00 337 84.00 19.98 338 83.75 20.76 339 82.65 21.04 340 85.68 21.60 341 80.72 19.79 342 84.08 21.21 343 85.18 21.39 344 77.18 19.58 345 57.68 14.83 346 68.90 17.24 347 77.25 18.94 348 83.41 18.18 349 86.21 18.69 350 69.84 15.38 351 74.90 17.65 352 81.14 20.59 353 85.38 20.25 354 79.57 17.43 355 85.63 18.68 356 82.42 18.16 357 86.25 20.75 358 82.26 20.01 359 84.45 20.14 360 82.26 19.56 361 84.01 20.11 362 84.17 20.52 363 82.05 18.59 364 82.05 18.26 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 193 cm % MAR 365 80.27 17.39 366 83.55 19.20 367 82.52 20.26 368 69.38 15.57 369 70.82 16.51 370 85.89 19.95 371 86.49 20.29 372 84.26 20.52 373 80.57 19.37 374 83.00 20.32 375 82.06 20.61 376 84.47 21.20 377 82.43 20.81 378 81.99 21.05 379 77.77 20.19 380 80.64 20.39 381 81.33 20.78 382 85.40 21.51 383 80.72 20.48 384 78.55 20.42 385 77.73 20.57 386 84.03 21.97 387 80.84 21.42 388 84.26 21.99 389 80.56 20.47 390 84.74 21.84 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. MAR 194 Appendix F: Percentage and MAR of Biogenic Opal in all cores (MAR values in mg/cm2/year) Alfonso Basin Pescadero Basin Alfonso Basin Pescadero Basin CP NH01-15 NH01-26 CP NH01-15 NH01-26 cm % MAR % MAR cm % MAR cm % MAR % MAR cm % MAR 1 4.30 0.42 4.66 0.58 1 15.72 3.23 50 4,83 0.71 4.78 0.53 50 14.03 2.81 2 4.29 0.42 5.23 0.64 2 14.91 2.90 51 4.70 0.70 4.85 0.58 51 13.17 2.44 3 4.50 0.45 5.20 0.60 3 15.46 2.77 52 4.62 0.69 4.98 0.62 52 16.32 3.06 4 4.41 0.45 5.47 0.63 4 16.19 2.72 53 5.14 0.77 5.64 0.75 53 13.84 2.51 5 4.42 0.46 5.37 0.62 5 15.47 2.69 54 5.22 0.78 5.12 0.63 54 14.07 2.76 6 4.41 0.47 5.11 0.57 6 13.15 2.18 55 4.64 0.70 5.04 0.61 55 15.02 2.68 7 4.57 0.49 4.81 0.52 7 14.27 2.39 56 4.86 0.73 4.53 0.60 56 13.38 2.71 8 5.03 0.55 5.02 0.54 8 13.75 2.30 57 4.34 0.66 4.68 0.59 57 15.10 2.81 9 5.39 0.60 5.03 0.55 9 15.49 2.41 58 3.86 0.59 5.06 0.60 58 12.60 2.21 10 4.63 0.52 5.78 0.64 10 15.60 2.51 59 4.30 0.66 4.80 0.59 59 11.89 2.19 11 4.28 0.49 4.99 0.55 11 15.40 2.69 60 4.62 0.71 4.09 0.53 60 13.33 2.57 12 5.43 0.63 5.04 0.71 12 14.61 3.32 61 4.34 0.67 4.77 0.64 61 13.74 2.74 13 5.19 0.61 5.32 0.74 13 14.33 3.08 62 5.13 0.79 4.84 0.65 62 13.84 2.86 14 4.75 0.57 6.46 0.78 14 13.66 2.81 63 3.12 0.48 4.82 0.65 63 14.50 2.70 15 4.32 0.52 4.74 0.57 15 13.90 2.92 64 4.10 0.64 4.76 0.62 64 16.00 3.04 16 4.93 0.61 4.66 0.55 16 14.05 2.85 65 4.14 0.64 4.21 0.49 65 13.82 2.29 17 4.23 0.53 4.43 0.52 17 15.73 3.03 66 4.49 0.70 4.63 0.56 66 12.64 2.20 18 4.30 0.54 4.86 0.55 18 14.64 2.68 67 4.62 0.72 4.49 0.56 67 12.94 2.11 19 4.26 0.55 5.87 0.62 19 15.84 2.85 68 4.10 0.65 4.43 0.57 68 13.26 2.57 20 4.20 0.55 5.43 0.57 20 16,76 2.65 69 4.13 0.65 4.59 0.59 69 14.21 2.71 21 4.14 0.55 4.89 0.53 21 14.54 2.41 70 4.01 0.64 4.87 0.60 70 11.87 2.28 22 4.60 0.61 5.12 0.55 22 15.02 2.62 71 3.83 0.61 4.44 0.56 71 12.65 2.51 23 5.00 0.67 5.52 0.59 23 13.95 2.33 72 4.49 0.72 4.50 0.59 72 14.50 2.96 24 5.00 0.67 5.72 0.60 24 14.23 2.50 73 5.39 0.86 5.29 0.72 73 14.13 2.90 25 5.46 0.73 5.42 0.58 25 14.74 2.63 74 4.98 0.80 4.54 0.56 74 13.49 2.60 26 4.47 0.60 4.86 0.50 26 15.37 2.68 75 4.69 0.76 4.36 0.56 75 14.05 2,67 27 4.79 0.65 5.19 0.51 27 15.19 2.64 76 4.54 0.73 4.08 0.53 76 14.15 2.74 28 5.00 0.68 4.67 0.51 28 15.83 2.81 77 5.09 0.82 4.28 0.54 77 14.28 2.65 29 5.21 0.71 4.64 0.49 29 14.28 2.62 78 5.21 0.85 4.83 0.67 78 14.32 2.70 30 4.35 0.60 5.21 0.55 30 16.24 2.89 79 4.92 0.80 4.70 0.63 79 14.30 2.57 31 4.66 0.64 4.82 0.54 31 15.66 2.89 80 4.30 0.70 4.62 0.60 80 14.52 2.48 32 4.89 0.67 5.26 0.58 32 16.41 2.95 81 4.09 0.67 5.14 0.68 81 12.79 2.32 33 5.10 0.71 5.72 0.65 33 16.72 3.03 82 4.44 0.73 5.22 0.66 82 13.35 2.21 34 4.50 0.63 4.58 0.53 34 14.05 2.54 83 4.25 0.70 4.64 0.58 83 13.08 2.41 35 5.26 0.73 5.10 0.56 35 14.06 2.41 84 4.06 0.67 4.86 0.65 84 15.21 2.94 36 5.03 0.70 6.57 0.70 36 15.40 2.95 85 4.03 0.67 4.34 0.56 85 12.76 2.29 37 5.64 0.79 4.63 0.52 37 14.34 2.61 86 3.99 0.67 3.86 0.53 86 11.92 2.18 38 4.79 0.68 4.57 0.48 38 15.21 2.69 87 5.04 0.84 4.30 0.61 87 12.41 2.07 39 5.58 0.79 4.33 0.47 39 13.72 2.33 88 4.60 0.77 4.62 0.67 88 12.83 2.50 40 4.37 0.62 4.52 0.53 40 13.45 2.32 89 4.09 0.69 4.34 0.60 89 14.42 2.53 41 4.46 0.64 4.63 0.52 41 13.58 2.19 90 4.51 0.76 5.13 0.70 90 13.86 2.94 42 5.87 0.84 4.67 0.50 42 12.81 2.45 91 4.45 0.76 3.12 0.32 91 14.41 2.78 43 4.54 0.65 4.92 0.56 43 14.00 2.37 92 4.16 0.71 4.10 0.44 92 13.29 2.42 44 4.80 0.69 4.92 0.56 44 13.97 2.57 93 3.72 0.64 4.14 0,60 93 12.55 2.43 45 4.58 0.66 5.00 0.57 45 13.03 2.39 94 4.28 0.73 4.49 0.62 94 11.26 1.89 46 4.51 0.66 4.74 0.52 46 13.04 2.31 95 3.50 0.60 4.62 0.69 95 12.28 2.21 47 5.00 0.73 5.07 0.57 47 14.27 2.72 96 3.19 0.55 4.10 0.55 96 13.50 2.68 48 5.01 0.73 4.96 0.54 48 13.23 2.64 97 3.81 0.66 4.13 0.56 97 12.68 2.54 49 5.94 0.87 5.02 0.58 49 14.57 2.96 98 3.95 0.69 4.01 0.57 98 13.59 2.71 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 195 cm % MAR % MAR cm % MAR cm % MAR % MAR cm % MAR 99 4.57 0.79 3.83 0.56 99 13.92 2.94 153 5.01 1.01 4.26 0.88 153 12.89 3.19 100 4.27 0.74 4.49 0.66 100 12.37 2.48 154 4.23 0.86 4.92 1.05 154 13.75 3.21 101 4.47 0.78 5.39 0.78 101 10.98 2.08 155 4.27 0.87 4.83 0.94 155 12.33 2.81 102 4.83 0.85 4.98 0.73 102 12.48 2.36 156 4.63 0.95 3.92 0.74 156 12.36 2.79 103 4.48 0.79 4.69 0.67 103 12.88 2.77 157 4.45 0.91 4.36 0.84 157 12.87 2.76 104 4.32 0.76 4.54 0.67 104 13.22 2.80 158 3.96 0.81 4.37 0.84 158 15.39 3.63 105 4.63 0.82 5.09 0.72 105 12.69 2.50 159 5.26 1.08 4.63 0.93 159 14.49 3.56 106 4.43 0.79 5.21 0.76 106 12.67 2.47 160 4.24 0.87 5.02 1.01 160 16.15 3.91 107 4.45 0.79 4.92 0.76 107 12.95 2.58 161 4.77 0.99 4.34 0.88 161 13.55 3.28 108 4.59 0.82 4.30 0.62 108 14.58 2.78 162 4.47 0.93 3.65 0.74 162 14.13 3.37 109 4.27 0.77 4.09 0.58 109 13.69 2.56 163 4.88 1.01 4.20 0.85 163 12.59 3.04 110 4.35 0.78 4.44 0.67 110 14.40 2.67 164 3.95 0.82 4.03 0.80 164 12.00 2.88 111 4.31 0.78 4.25 0.61 111 15.22 2.89 165 3.81 0.80 4.19 0.82 165 14.37 3.28 112 4.16 0.75 4.06 0.62 112 12.56 2.22 166 4.26 0.89 4.51 0.83 166 15.23 3.86 113 4.56 0.83 4.03 0.58 113 13.66 2.53 167 4.30 0.90 4.97 0.91 167 16.05 4.15 114 4.65 0.85 3.99 0.60 114 12.93 2.36 168 4.41 0.93 4.65 0.86 168 18.12 4.37 115 4.14 0.75 5.04 0.73 115 12.90 2.45 169 5.53 1.17 4.79 0.93 169 17.62 3.78 116 4.11 0.75 4.60 0.69 116 13.85 2.75 170 5.03 1.06 4.44 0.80 170 12.65 2.41 117 4.28 0.78 4.09 0.61 117 12.67 2.80 171 4.50 0.96 4.43 0.78 171 14.67 2.12 118 4.63 0.85 4.51 0.69 118 10.55 2.16 172 4.57 0.97 4.01 0.70 172 14.18 2.08 119 4.45 0.82 4.45 0.64 119 12.20 2.54 173 5.27 1.12 3.57 0.64 173 13.98 2.86 120 5.78 1.07 4.16 0.63 120 12.51 2.86 174 3.92 0.84 3.54 0.66 174 13.31 3.04 121 4.44 0.82 3.72 0.59 121 13.12 2.79 175 4.25 0.91 3.99 0.76 175 14.08 3.21 122 4.25 0.79 4.28 0.68 122 13.15 2.81 176 4.62 0.99 3.94 0.70 176 11.57 2.58 123 4.58 0.85 3.50 0.52 123 14.65 2.95 177 4.15 0.89 4.47 0.80 177 11.43 2.46 124 4.95 0.93 3.19 0.58 124 12.13 2.53 178 4.79 1.03 4.15 0.78 178 10.54 2.22 125 4.85 0.91 3.81 0.70 125 12.60 2.48 179 4.20 0.91 4.26 0.79 179 11.43 2.53 126 4.71 0.89 3.95 0.69 126 11.78 2.56 180 4.99 1.08 4.65 0.91 180 11.06 2.57 127 5.70 1.08 4.57 0.80 127 14.51 2.95 181 5.16 1.12 4.79 0.97 181 11.16 2.53 128 5.11 0.97 4.27 0.73 128 12.10 2.49 182 4.63 1.01 5.06 0.96 182 11.82 2.65 129 4.50 0.85 4.87 0.85 129 12.01 2.55 183 5.70 1.25 5.35 0.99 183 13.06 3.04 130 4.27 0.81 5.49 0.94 130 13.15 2.87 184 4.05 0.89 4.65 0.85 184 10.97 2.51 131 5.61 1.07 4.75 0.84 131 9.89 2.04 185 5.67 1.25 4.29 0.83 185 11.87 2.52 132 5.04 0.96 4.75 0.86 132 13.48 2.70 186 4.91 1.08 4.88 0.90 186 11,96 2.70 133 4.94 0.95 4.58 0.79 133 13.87 2.88 187 4.76 1.05 4.08 0.82 187 11.37 2.77 134 5.13 0.99 4.73 0.81 134 12.27 2.39 188 5.01 1.11 5.76 1.08 188 11.12 2.60 135 4.54 0.88 4.41 0.83 135 11.94 2.66 189 4.93 1.09 4.64 0.89 189 12.00 2.50 136 4.51 0.87 4.26 0.79 136 10.90 2.29 190 5.32 1.18 4.55 0.88 190 14.15 3.23 137 4.84 0.94 4.25 0.73 137 11.56 2.48 191 4.34 0.97 4.37 0.84 191 13.31 2.87 138 5.20 1.01 4.37 0.79 138 12.12 2.69 192 4.26 0.95 4.43 0.90 192 11.80 2.61 139 5.57 1.09 4.44 0.83 139 13.67 2.95 193 4.44 0.99 4.29 0.83 193 13.06 2.89 140 4.03 0.79 4.51 0.86 140 12.77 2.64 194 4.81 1.08 4.44 0.87 194 12.46 2.82 141 5.38 1.05 4.52 0.83 141 13.40 2.83 195 4.61 1.04 3.77 0.74 195 13.83 3.12 142 4.21 0.83 4.48 0.83 142 13.77 2,97 196 4.90 1.11 2.45 0.46 196 12.20 2.61 143 4.20 0.83 4.94 0.93 143 14.46 2.85 197 4.30 0.97 5.10 0.87 197 10.93 2.39 144 4.82 0.95 4.35 0.77 144 11.74 2.31 198 4.35 0.99 5.16 1.00 198 10.99 2.30 145 3.74 0.74 3.79 0.69 145 13.59 2.74 199 0.00 0.00 5.02 0.93 199 11.00 2.55 146 3.92 0.78 3.79 0.70 146 12.91 2.52 200 4.24 0.97 4.67 0.95 200 13.06 2.91 147 3.95 0.79 4.40 0.84 147 11.17 2.44 201 4.74 1.08 4.30 0.94 201 12.10 2.70 148 4.69 0.94 4.74 0.92 148 12.46 2.62 202 5.03 1.15 4.42 1.08 202 11.89 2.80 149 4.21 0.84 4.64 0.94 149 13.54 2.95 203 4.25 0.98 5.16 1.18 203 12.44 2.73 150 4.24 0.85 5.09 1.12 150 12.40 2.71 204 4.23 0.97 5.04 1.19 204 11.56 2.54 151 4.20 0.85 4.54 0.95 151 15.78 3.58 205 5.01 1.15 5.31 1.19 205 17.48 3.82 152 4.27 0.86 4.21 0.85 152 13.59 3.24 206 4.62 1.07 5.14 1.11 206 12.56 2.93 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 196 cm % MAR % MAR cm % MAR cm % MAR % MAR cm % MAR 207 4.89 1.13 5.32 1.01 207 11.31 2.62 263 13.07 3.12 208 4.82 1.12 5.19 0.98 209 12.64 2.94 264 12.74 2.97 209 4.56 1.06 5,65 1.11 210 12.15 2.85 265 14.67 3.28 210 4.96 1.16 5.10 1.01 211 11.78 2.74 266 15,21 3.44 211 4.69 1.09 5.77 1.15 212 12.20 2.80 267 13.95 3.30 212 4.96 1.16 4.94 0.98 213 13.92 3.20 268 14.39 3.23 213 4.95 0.83 214 18.21 4.04 269 13.49 3.10 214 5.22 0.91 215 14.77 3.09 270 15.45 3.44 215 4.83 0.80 216 14.27 2.94 271 13.07 2.94 216 4.96 1.00 217 12.63 2.74 272 14.56 3.32 217 5.06 0.95 218 12.69 2.73 273 14.52 3.35 218 5.15 1.05 219 14.46 3.09 274 14.22 3.24 219 4.74 1.01 220 12.02 2.57 275 12.73 2.91 220 5.05 1.08 221 11.52 2.40 276 12.07 2.77 221 4.73 1.01 222 11.44 2.64 277 12.95 2.99 222 4.99 1.08 223 8.53 1.88 278 12.58 2.83 223 5.10 1.06 224 11.76 2.66 279 12.76 2.87 224 5.28 1.07 225 12.03 2.59 280 13.01 3.16 225 5.14 1.02 226 13.10 2.91 281 12.95 2.96 226 5.27 1.04 227 14.20 3.33 282 13.22 2.93 227 5.17 1.02 228 13.91 3.28 283 13.57 3.04 228 5.00 0.99 229 14.12 3.43 284 10.92 2.55 229 4.80 0.91 230 15.19 3.55 285 12.38 2.82 230 4.62 0.92 231 13.09 2.80 286 11.93 2.74 231 5.02 1.00 232 14.48 3.26 287 14.17 3.42 232 5.39 1.10 233 13.90 2.93 288 12.74 3.13 233 4.58 0.88 234 12.44 2.53 289 19.52 4.82 234 5.17 1.04 235 11.43 2.54 290 13.20 3.20 235 4.86 0.97 236 12.15 2.69 291 11.71 2.67 236 5.20 1.04 237 14.10 3.26 292 12.01 2.81 237 4.46 0.88 238 15.18 3.57 293 13.79 3.34 238 4.70 0.92 239 13.14 2.95 294 12.91 3.17 240 12.40 2.89 295 9.99 2.48 241 13.72 3.24 296 12.04 3.08 242 13.68 3.35 297 14.65 3.55 243 13.97 3.37 298 14.15 3.35 244 11.76 2.86 299 13.34 3.14 245 13.28 3.12 300 12.69 3.05 246 12.93 2.90 301 12.74 3.05 247 12.80 2.79 302 13.41 3.10 248 14.70 3.33 303 15.75 3.80 249 13.85 3.10 304 16.25 3.94 250 13.05 2.82 305 13.73 3.45 251 13.37 3.09 306 13.84 3.48 253 12.77 3.02 307 11.73 3.13 254 13.17 3.14 308 13.02 3.01 255 12.80 3.09 309 14.04 3.15 256 12.92 3.00 310 14.46 3.62 257 15.25 3.47 311 13.93 3.64 258 11.65 2.69 312 13.82 3.65 259 16.34 3.89 313 13.34 3.44 260 12.19 2.92 314 13.17 3.40 261 16.60 3.73 315 13.63 2.98 262 13.56 3.03 316 13.79 3.02 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. cm 197 MAR cm % MAR cm % MAR % MAR cm % MAR 317 12.58 2.93 371 17.35 4.04 318 21.09 5.21 372 10.54 2.45 319 15.78 4.02 373 10.56 2.48 320 12.86 3.26 374 12.80 3.12 321 14.29 3.57 375 16.08 3.87 322 11.79 2.79 376 13.70 3.35 323 12.29 3,05 377 13.89 3.49 324 15.02 3.69 378 11.98 3.01 325 13.63 3.51 379 14.03 3.54 326 11.41 2.92 380 13.53 3.47 327 11.84 3.07 381 16.70 4.34 328 13.02 3.31 382 12.35 3.12 329 13.24 3.47 383 12.80 3.27 330 13.65 3.44 384 10.50 2.64 331 13.95 3.38 385 16.10 4.08 332 14.50 3.21 386 16.68 4.34 333 21.08 4.44 387 18.07 4.78 334 13.72 2.94 388 12.75 3.33 335 10.95 2.55 389 14.44 3.83 336 10.95 2.73 390 11.20 2.92 337 15.28 3.84 391 14.19 3.60 338 19.06 4.59 392 10.47 2.70 339 12.68 3.02 340 13.12 3.25 341 14.38 3.66 342 10.79 2.72 343 14.84 3.64 344 12.08 3.05 345 10.33 2.59 346 16.79 4.26 347 16.46 4.23 348 15.42 3.86 349 12.77 3.13 350 12.76 2.78 351 10.66 2.31 352 13.46 2.96 353 13.77 3.24 354 11.11 2.82 355 9.19 2.18 356 15.12 3.31 357 9.34 2.04 358 13.45 2,96 359 9.98 2.40 360 13.66 3.32 361 11.52 2.75 362 13.23 3.15 363 11.83 2.83 364 11.92 2.91 365 13.76 3.12 366 11.76 2.62 367 13.99 3.03 368 12.63 2.90 369 12.76 3.13 370 14.18 3.18 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 198 Appendix G: Percentage and MAR of Total Carbon in all cores (MAR values in mg/cm2/year) Alfonso Basin Pescadero Basin Alfonso Basin Pescadero Basin cm NH01-15 cm NH01-26 cm NH01-15 cm NH01-26 cm % MAR cm % MAR cm % MAR cm % MAR 1 7.42 0.93 1 3.97 0.82 50 6.58 0.7236 50 4.12 0.83 2 6.92 0.84 2 4.26 0.83 51 6.61 0.7852 51 4.24 0.79 3 6.95 0.80 3 4.08 0.73 52 6.59 0.8163 52 4.13 0.78 4 6.82 0.78 4 4.08 0.68 53 6.62 0.8832 53 3.96 0.72 5 7.08 0.82 5 3.87 0.67 54 6.84 0.8427 54 3.87 0.76 6 7.11 0.79 6 3.81 0.63 55 6.73 0.8201 55 3.83 0.68 7 7.64 0.83 7 4.01 0.67 56 6.71 0.8913 56 4.05 0.82 8 7.83 0,34 8 4.05 0.68 57 6.72 0.8531 57 4.06 0.76 9 8.02 0.88 9 4.15 0.65 58 6.62 0.7801 58 4.03 0.71 10 7.39 0.82 10 3.96 0.64 59 6.76 0.8347 59 3.67 0.68 11 7.64 0.84 11 3.83 0.67 60 6.63 0.866 60 3.68 0.71 12 6.18 0.87 12 3.83 0.87 61 6.74 0.9038 61 3.69 0.73 13 5.67 0.79 13 3.58 0.77 62 6.57 0.8804 62 3.95 0.82 14 5.04 0.61 14 3.85 0.79 63 6.63 0.891 63 3.72 0.69 15 6.72 0,80 15 3.70 0.78 64 6.69 0.8738 64 3.68 0.70 16 6.60 0.77 16 4.11 0.83 65 6.75 0.7884 65 3.85 0.64 17 6.99 0.82 17 4.19 0.81 66 6.77 0.8217 66 3.56 0.62 18 7.03 0.80 18 3.76 0.69 67 6.83 0.8447 67 3.72 0.61 19 6.79 0.72 19 3.99 0.72 68 6.39 0.8167 68 3.80 0.74 20 6.85 0.72 20 3.90 0.62 69 6.33 0.8164 69 3.77 0.72 21 6.84 0.73 21 3.73 0.62 70 6.76 0.8347 70 3.68 0.71 22 7.12 0.77 22 4.07 0.71 71 6.54 0.8296 71 4.07 0.81 23 6.97 0.75 23 3.74 0.63 72 6.41 0.8416 72 3.72 0.76 24 7.20 0.76 24 3.87 0.68 73 6.61 0.898 73 3.91 0.80 25 6.97 0.74 25 3.86 0.69 74 6.87 0.8503 74 4.02 0.78 26 6.76 0.70 26 4.01 0.70 75 6.84 0.8802 75 4.06 0.77 27 6.97 0.68 27 3.59 0.62 76 7.03 0.9148 76 4.17 0.81 28 6.70 0.74 28 3.69 0.65 77 6.89 0.8726 77 3.99 0.74 29 7.01 0.75 29 3.83 0.70 78 6.65 0.919 78 4.03 0.76 30 7.20 0.76 30 3.61 0.64 79 6.70 0.8985 79 3.93 0.71 31 7.21 0.80 31 3.60 0.66 80 6.49 0.8414 80 4.02 0.69 32 7.18 0.79 32 3.98 0.71 81 6.77 0.898 81 3.70 0.67 33 7.35 0.83 33 3.85 0.70 82 6.60 0.8404 82 3.41 0.56 34 6.79 0.79 34 3.96 0.71 83 6.83 0.8473 83 3.68 0.68 35 6.83 0.75 35 3.96 0.68 84 6.81 0.9106 84 3.66 0.71 36 7.05 0.75 36 3.92 0.75 85 7.40 0.9479 85 3.66 0.66 37 7.16 0.80 37 3.98 0.72 86 7.21 0.9865 86 3.46 0.63 38 7.60 0.80 38 4.02 0.71 87 6.51 0.9168 87 3.34 0.56 39 7.18 0.77 39 4.02 0.68 88 6.41 0.9247 88 3.34 0.65 40 7.39 0.86 40 3.89 0.67 89 6.87 0.9567 89 3.72 0.65 41 7.80 0.8777 41 4.02 0.65 90 6.41 0.8795 90 3.73 0.79 42 7.26 0.7786 42 3.82 0.73 91 5.49 0.5645 91 3.48 0.67 43 7.12 0.8133 43 3.86 0.65 92 6.73 0.723 92 3.88 0.71 44 7.05 0.8047 44 3.74 0.69 93 6.38 0.9173 93 3.84 0.74 45 7.00 0.7936 45 3.70 0.68 94 6.38 0.8817 94 3.69 0.62 46 6.94 0.7613 46 3.82 0.68 95 6.92 1.0317 95 3.66 0.66 47 6.99 0.7839 47 3.82 0.73 96 7.19 0.9642 96 3.74 0.74 48 6.91 0.7488 48 4.18 0.83 97 7.09 0.9577 97 3.37 0.67 49 7.32 0.8452 49 3.76 0.76 98 7.51 1.0613 98 3.46 0.69 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 199 cm % MAR 99 6.98 1.0269 100 6.38 0.9386 101 6.40 0.9239 102 6.97 1.0268 103 6.44 0.9183 104 5.80 0.8567 105 6.64 0.9429 106 6.66 0.9719 107 6.22 0.9619 108 6.08 0.8694 109 6.22 0.8827 110 6.21 0.9357 111 6.49 0.9376 112 6.18 0.9379 113 6.40 0.9264 114 6.34 0.9522 115 5.90 0.8512 116 6.27 0.9466 117 6.62 0.9929 118 6.57 1.0095 119 6.17 0.8901 120 6.11 0.9303 121 6.23 0.9852 122 6.42 1.0224 123 7.92 1.1683 124 7.47 1.3623 125 7.72 1.4299 126 6.76 1.1811 127 5.91 1.0291 128 6.11 1.0425 129 6.08 1.0545 130 6.11 1.0482 131 5.95 1.0543 132 6.03 1.0869 133 6.07 1.0421 134 6.31 1.0855 135 6.25 1.1799 136 6.20 1.1549 137 7.36 1.2704 138 6.94 1.2534 139 7.11 1.3245 140 6.32 1.2029 141 6.14 1.1227 142 5.63 1.0428 143 5.75 1.0779 144 7.72 1.3751 145 7.88 1.425 146 7.17 1.3212 147 6.72 1.2782 148 6.64 1.2828 149 6.11 1.2332 150 5.50 1.207 151 5.92 1.2385 152 6.90 1.4026 cm % MAR 99 3.72 0.78 100 3.56 0.71 101 3.00 0.57 102 3.39 0.64 103 3.86 0.83 104 3.98 0.84 105 3.67 0.72 106 4.01 0.78 107 4.09 0.82 108 3.84 0.73 109 4.07 0.76 110 3.82 0.71 111 4.07 0.77 112 3.58 0.63 113 3.83 0.71 114 3.56 0.65 115 3.27 0.62 116 3.43 0.68 117 3.45 0.76 118 3.01 0.62 119 3.07 0.64 120 3.24 0.74 121 3.68 0.78 122 3.49 0.74 123 3.70 0.75 124 3.65 0.76 125 3.66 0.72 126 3.72 0.81 127 3.51 0.71 128 3.36 0.69 129 3.96 0.84 130 3.84 0.84 131 3.67 0.76 132 3.84 0.77 133 3.36 0.70 134 3.61 0.70 135 3.62 0.81 136 3.47 0.73 137 3.68 0.79 138 3.96 0.88 139 3.80 0.82 140 3.97 0.82 141 4.49 0.95 142 4.16 0.90 143 3.56 0.70 144 3.48 0.68 145 3.45 0.70 146 3.60 0.70 147 3.47 0.76 148 3.43 0.72 149 3.38 0.73 150 3.20 0.70 151 3.37 0.76 152 3.56 0.85 cm % MAR 153 7.00 1.4466 154 6.67 1.419 155 6.24 1.2174 156 6.94 1.3068 157 6.31 1.2168 158 6.25 1.2052 159 5.95 1.2002 160 6.18 1.2474 161 6.49 1.3113 162 7.11 1.4401 163 7.44 1.5061 164 6.66 1.3273 165 6.64 1.2931 166 7.01 1.2851 167 6.08 1.1103 168 6.01 1.1096 169 5.62 1.0864 170 6.38 1.1507 171 6.53 1.1463 172 6.55 1.146 173 6.16 1.1045 174 6.59 1.2198 175 6.41 1.2246 176 6.61 1.165 177 7.05 1.255 178 7.08 1.3264 179 6.59 1.2276 180 6.85 1.3348 181 6.12 1.2367 182 6.03 1.1419 183 5.98 1.104 184 6.15 1.1231 185 5.62 1.0844 186 6.59 1.2206 187 6.54 1.316 188 5.88 1.1009 189 6.23 1.1939 190 6.98 1.3543 191 5.77 1.1161 192 5.50 1.1154 193 6.26 1.2124 194 6.16 1.2033 195 6.83 1.3424 196 5.94 1.1129 197 5.85 0.9975 198 4.90 0.9501 199 6.15 1.1325 200 5.60 1.1417 201 5.53 1.2055 202 4.79 1.1751 203 4.71 1.0755 204 4.63 1.0923 205 4.81 1.0822 206 5.42 1.1716 cm % MAR 153 3.68 0.91 154 3.76 0.88 155 3.70 0.84 156 3.76 0.85 157 3.70 0.79 158 3.65 0.86 159 3.70 0.91 160 3.51 0.85 161 3.61 0.87 162 3.72 0.89 163 3.63 0.88 164 3.28 0.79 165 3.46 0.79 166 3.53 0.89 167 2.61 0.68 168 3.49 0.84 169 3.38 0.73 170 3.66 0.70 171 3.38 0.49 172 3.40 0.50 173 3.23 0.66 174 3.33 0.76 175 3.52 0.80 176 3.57 0.79 177 3.45 0.74 178 3.83 0.81 179 3.63 0.80 180 3.57 0.83 181 3.38 0.76 182 3.58 0.80 183 3.44 0.80 184 3.08 0.71 185 3.26 0.69 186 3.52 0.80 187 3.58 0.87 188 3.86 0.90 189 4.03 0.84 190 3.80 0.87 191 3.77 0.81 192 3.64 0.80 193 3.56 0.79 194 3.29 0.75 195 3.61 0.82 196 3.12 0.67 197 3.51 0.77 198 3.75 0.79 199 3.97 0.92 200 4.09 0.91 201 3.77 0.84 202 3.65 0.86 203 3.49 0.77 204 3.36 0.74 205 4.59 1.00 206 3.54 0.83 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 2 0 0 cm % MAR cm % MAR 207 6.12 1.1597 207 3.13 0.73 208 6.02 1.1321 208.5 4.11 0.95 209 5.51 1.0803 210 3.87 0.91 210 6.40 1.2632 211 3.07 0.72 211 5.85 1.1666 212 3.34 0.77 212 6.50 1.2884 213 3.38 0.78 213 6.56 1.0971 214 3.47 0.77 214 5.85 1.0235 215 3.64 0.76 215 6.44 1.068 216 3.49 0.72 216 6.28 1.2614 217 3.27 0.71 217 6.22 1.1668 218 3.47 0.75 218 6.83 1.3859 219 3.38 0.72 219 6.68 1.4227 220 3.29 0.70 220 6.44 1.3726 221 3.32 0.69 221 6.27 1.3369 222 3.46 0.80 222 6.25 1.3563 223 3.47 0.76 223 6.42 1.3283 224 3.51 0.79 224 6.09 1.2291 225 3.48 0.75 225 5.92 1.1756 226 3.45 0.77 226 6.19 1.2225 227 3.65 0.86 227 6.17 1.2215 228 3.26 0.77 228 6.68 1.3209 229 3.37 0.82 229 7.12 1.3449 230 3.67 0.86 230 6.47 1.2887 231 3.61 0.77 231 6.18 1.2272 232 3.75 0.84 232 6.37 1.2987 233 3.82 0.81 233 6.56 1.2579 234 3.63 0.74 234 6.15 1.2435 235 3.57 0.79 235 6.14 1.2304 236 3.65 0.81 236 5.84 1.1667 237 3.33 0.77 237 6.69 1.3245 238 3.33 0.78 238 6.33 1.2373 239 3.35 0.75 240 3.62 0.84 241 3.67 0.87 242 3.84 0.94 243 3.47 0.84 244 3.73 0.91 245 3.92 0.92 246 4.06 0.91 247 3.87 0.84 248 3.84 0.87 249 3.71 0.83 250 3.67 0.79 251 3.72 0.86 252.5 3.98 0.94 253.5 3.71 0.89 254.5 3.86 0.93 255.5 3.32 0.77 256.5 3.88 0.88 257.5 3.79 0.87 258.5 3.75 0.89 259.5 3.37 0.81 260.5 3.63 0.82 261.5 3.70 0.83 cm % MAR cm % MAR 262.5 3.67 0.87 263.5 3.61 0.84 264.5 3.76 0.84 265.5 3.79 0.86 266.5 3.80 0.90 267.5 3.88 0.87 268.5 4.01 0.92 269.5 4,01 0.89 270.5 3.93 0.88 271.5 3.83 0.88 272.5 3.72 0.86 273.5 3.93 0.90 275 3.78 0.86 276 3.66 0.84 277 3.81 0.88 278 3.94 0.89 279 3.91 0.88 280 3.71 0.90 281 3.61 0.83 282 3.59 0.80 283 3.50 0.78 284 3.47 0.81 285 3.37 0.77 286 3.42 0.79 287 3.39 0.82 288 3.45 0.85 289 3.56 0.8 8 290 3.76 0.91 291 3.57 0.81 292 3.65 0.85 293 3.75 0.91 294 3.73 0.92 295 3.53 0.88 296 3.16 0.81 297 3.69 0.89 298 3.65 0.86 299 3.71 0.87 300 3.72 0.90 301 3.80 0.91 302 3.40 0.79 303 3.34 0.81 304 3.61 0.88 305 3.70 0.93 306 3.52 0.88 307 3.31 0.88 308 3.32 0.77 309 3.51 0.79 310 3.28 0.82 311 3.77 0.98 312 3.70 0.98 313 3.51 0.91 314 3.75 0.97 315 3.82 0.84 316 3.89 0.85 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 2 0 1 cm cm % MAR 317 3.95 0.92 318 3.73 0.92 319 3.72 0.95 320 3.64 0.92 321 3.61 0.90 322 3.73 0.88 323 3.38 0.84 324 3.94 0.97 325 3.41 0.88 326 2.66 0.68 327 2.98 0.77 328 3.22 0.82 329 3.21 0.84 330 3.08 0.78 331 3.25 0.79 332 3.33 0.74 333 3.24 0.68 334 3.28 0.70 335 3.03 0.71 336 3.44 0.86 337 3.59 0.90 338 3.34 0.80 339 3.20 0.76 340 3.05 0.76 341 2.86 0.73 342 3.40 0.86 343 3.22 0.79 344 3.24 0.82 345 3.13 0.79 346 3.64 0.92 347 5.58 1.43 348 4.34 1.09 349 3.63 0.89 350 3.18 0.69 351 2.94 0.64 352 4.30 0.95 353 3.89 0.92 354 3.75 0.95 355 3.13 0.74 356 3.27 0.72 357 3.21 0.70 358 3.18 0.70 359 2.88 0.69 360 3.30 0.80 361 3.01 0.72 362 3.12 0.74 363 3.20 0.77 364 3.38 0.82 365 3.26 0.74 366 3.41 0.76 367 3.53 0.77 368 3.12 0.72 369 3.48 0.85 370 4.67 1.05 cm % MAR 371 3.73 0.87 372 3.09 0.72 373 2.94 0.69 374 2.86 0.70 375 2.93 0.70 376 2.61 0.64 377 2.78 0.70 378 2.72 0.68 379 2.85 0.72 380 3.05 0.78 381 3.07 0.80 382 3.47 0.88 383 3.04 0.78 384 3.18 0.80 385 3.17 0.80 386 3.93 1.02 387 3.02 0.80 388 3.06 0.80 389 3.36 0.89 390 3.10 0.81 391 3.11 0.79 392 3.21 0.83 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 2 0 2 Appendix H: Percentage and MAR of Organic Carbon in all cores (MAR values in mg/cm2/year) Alfonso Basin Pescadero Basin Alfonso Basin Pescadero Basin CP NH01-15 NH01-26 CP NH01-15 NH01-26 cm % MAR % MAR cm % MAR cm % MAR % MAR cm % MAR 1 5.61 0.55 5.61 0.70 1 3.31 0.68 42 6.15 0.86 6.15 0.66 42 3.47 0.66 2 5.64 0.58 5.64 0.69 2 3.56 0.69 43 6.01 0.81 6.01 0.69 43 3.51 0.59 3 5.90 0.61 5.90 0.68 3 3.46 0.62 44 5.64 0.78 5.64 0.64 44 3.37 0.62 4 6.05 0.66 6.05 0.69 4 3.54 0.59 45 5.43 0.81 5.43 0.62 45 3.26 0.60 5 6.42 0.66 6.42 0.74 5 3.36 0.58 46 5.57 0.86 5.57 0.61 46 3.37 0.60 6 6.35 0.68 6.35 0.71 6 3.24 0.54 47 5.88 0.84 5.88 0.66 47 3.30 0.63 7 6.47 0.72 6.47 0.70 7 3.38 0.57 48 5.78 0.89 5.78 0.63 48 3.77 0.75 8 6.67 0.75 6.67 0.71 8 3.48 0.58 49 6.09 0.74 6.09 0.70 49 3.51 0.71 9 6.85 0.71 6.85 0.75 9 3.63 0.56 50 5.06 0.76 5.06 0.56 50 3.77 0.76 10 6.44 0.76 6.44 0.72 10 3.44 0.55 51 5.14 0.78 5.14 0.61 51 3.86 0.72 11 6.74 0.63 6.74 0.74 11 3.24 0.57 52 5.25 0.82 5.25 0.65 52 3.78 0.71 12 5.50 0.58 5.50 0.78 12 3.32 0.76 53 5.49 0.84 5.49 0.73 53 3.54 0.64 13 4.98 0.53 4.98 0.69 13 3.09 0.66 54 5.62 0.80 5.62 0.69 54 3.52 0.69 14 4.53 0.69 4.53 0.55 14 3.29 0.68 55 5.33 0.78 5.33 0.65 55 3.51 0.63 15 5.79 0.68 5.79 0.69 15 3.21 0.68 56 5.18 0.83 5.18 0.69 56 3.60 0.73 16 5.63 0.67 5.63 0.66 16 3.59 0.73 57 5.51 0.84 5.51 0.70 57 3.59 0.67 17 5.47 0.71 5.47 0.64 17 3.86 0.75 58 5.57 0.79 5.57 0.66 58 3.62 0.63 18 5.67 0.72 5.67 0.64 18 3.53 0.65 59 5.21 0.79 5.21 0.64 59 3.33 0.61 19 5.72 0.71 5.72 0.61 19 3.70 0.67 60 5.21 0.76 5.21 0.68 60 3.50 0.67 20 5.55 0.72 5.55 0.58 20 3.69 0.58 61 4.99 0.80 4.99 0.67 61 3.62 0.72 21 5.52 0.76 5.52 0.59 21 3.51 0.58 62 5.24 0.77 5.24 0.70 62 3.87 0.80 22 5.73 0.75 5.73 0.62 22 3.82 0.67 63 5.01 0.85 5.01 0.67 63 3.65 0.68 23 5.66 0.80 5.66 0.61 23 3.50 0.59 64 5.53 0.79 5.53 0.72 64 3.55 0.67 24 6.00 0.76 6.00 0.63 24 3.61 0.63 65 5.12 0.85 5.12 0.60 65 3.59 0.59 25 5.69 0.73 5.69 0.61 25 3.52 0.63 66 5.44 0.88 5.44 0.66 66 3.20 0.56 26 5.40 0.74 5.40 0.56 26 3.64 0.63 67 5.66 0.86 5.66 0.70 67 3.33 0.54 27 5.51 0.73 5.51 0.54 27 3.32 0.58 68 5.48 0.89 5.48 0.70 68 3.66 0.71 28 5.37 0.75 5.37 0.59 28 3.51 0.62 69 5.66 0.96 5.66 0.73 69 3.34 0.64 29 5.53 0.78 5.53 0.59 29 3.59 0.66 70 6.07 0.90 6.07 0.75 70 3.19 0.61 30 5.69 0.81 5.69 0.60 30 3.43 0.61 71 5.70 0.86 5.70 0.72 71 3.56 0.71 31 5.91 0.81 5.91 0.66 31 3.36 0.62 72 5.44 0.89 5.44 0.71 72 3.35 0.68 32 5.88 0.79 5.88 0.64 32 3.72 0.67 73 5.59 0.97 5.59 0.76 73 3.56 0.73 33 5.74 0.76 5.74 0.65 33 3.61 0.65 74 6.06 0.92 6.06 0.75 74 3.69 0.71 34 5.51 0.81 5.51 0.64 34 3.71 0.67 75 5.74 0.91 5.74 0.74 75 3.74 0.71 35 5.81 0.83 5.81 0.64 35 3,73 0.64 76 5.64 0.93 5.64 0.73 76 3.90 0.75 36 5.92 0.81 5.92 0.63 36 3.76 0.72 77 5.73 0.85 5.73 0.73 77 3.79 0.70 37 5.76 0.91 5.76 0.65 37 3.77 0.69 78 5.27 0.88 5.27 0.73 78 3.90 0.73 38 6.44 0.74 6.44 0.68 38 3.77 0.67 79 5.39 0.87 5.39 0.72 79 3.84 0.69 39 5.25 0.74 5.25 0.57 39 3.69 0.63 80 5.34 0.90 5.34 0.69 80 3.90 0.67 40 5.22 0.89 5.22 0.61 40 3.54 0.61 81 5.52 0.91 5.52 0.73 81 3.58 0.65 41 6.23 0.88 6.23 0.70 41 3.67 0.59 82 5.57 0.88 5.57 0.71 82 3.28 0.54 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 203 cm % MAR % 83 5.37 0.98 5.37 84 5.90 0.97 5.90 85 5.83 0.92 5.83 86 5.55 0.89 5.55 87 5.36 0.93 5.36 88 5.53 0.96 5.53 89 5.70 0.93 5.70 90 5.50 0.75 5.50 91 4.43 0.81 4.43 92 4.77 0.82 4.77 93 4.80 0.95 4.80 94 5.57 0.95 5.57 95 5.53 0.98 5.53 96 5.71 0.93 5.71 97 5.38 0.91 5.38 98 5.28 0.86 5.28 99 4.97 0.92 4.97 100 5.31 0.94 5.31 101 5.37 1.02 5.37 102 5.83 0.91 5.83 103 5.20 0.82 5.20 104 4.66 0.99 4.66 105 5.59 0.90 5.59 106 5.11 0.83 5.11 107 4.66 0.87 4.66 108 4.86 0.86 4.86 109 4.84 0.83 4.84 110 4.62 0.88 4.62 111 4.90 0.84 4.90 112 4.66 0.81 4.66 113 4.49 0.89 4.49 114 4.89 0.80 4.89 115 4.42 0.88 4.42 116 4.82 0.80 4.82 117 4.35 0.81 4.35 118 4.42 0.89 4.42 119 4.86 0.73 4.86 120 3.98 0.73 3.98 121 3.92 0.74 3.92 122 3.97 0.84 3.97 123 4.54 0.73 4.54 124 3.93 0.87 3.93 125 4.64 0.82 4.64 126 4.37 0.89 4.37 127 4.75 0.89 4.75 128 4.70 0.90 4.70 129 4.73 0.90 4.73 MAR cm % MAR 0.67 83 3.58 0.66 0.79 84 3.56 0.69 0.75 85 3.57 0.64 0.76 86 3.31 0.61 0.75 87 3.17 0.53 0.80 88 3.18 0.62 0.79 89 3.57 0.63 0.75 90 3.64 0.77 0.46 91 3.39 0.65 0.51 92 3.73 0.68 0.69 93 3.52 0.68 0.77 94 3.29 0.55 0.82 95 3.27 0.59 0.77 96 3.39 0.67 0.73 97 3.17 0.63 0.75 98 3.30 0.66 0.73 99 3.57 0.75 0.78 100 3.42 0.69 0.78 101 2.70 0.51 0.86 102 3.15 0.60 0.74 103 3.54 0.76 0.69 104 3.63 0.77 0.79 105 3.40 0.67 0.75 106 3.80 0.74 0.72 107 3.88 0.77 0.69 108 3.71 0.71 0.69 109 3.90 0.73 0.70 110 3.65 0.68 0.71 111 3.85 0.73 0.71 112 3.29 0.58 0.65 113 3.48 0.65 0.73 114 3.20 0.59 0.64 115 2.92 0.55 0.73 116 3.08 0.61 0.65 117 3.13 0.69 0.68 118 2.65 0.54 0.70 119 2.77 0.58 0.61 120 2.92 0.67 0.62 121 3.26 0.69 0.63 122 3.09 0.66 0.67 123 3.30 0.66 0.72 124 3.15 0.66 0.86 125 3.31 0.65 0.76 126 3.44 0.75 0.83 127 3.23 0.66 0.80 128 3.09 0.64 0.82 129 3.66 0.78 cm % MAR % 130 4.76 0.82 4.76 131 4.33 0.84 4.33 132 4.41 0.89 4.41 133 4.66 0.89 4.66 134 4.61 0.78 4.61 135 4.05 0.83 4.05 136 4.32 0.95 4.32 137 4.89 0.83 4.89 138 4.27 0.83 4.27 139 4.24 0.77 4.24 140 3.93 0.88 3.93 141 4.50 0.86 4.50 142 4.37 0.76 4.37 143 3.89 0.86 3.89 144 4.35 0.85 4.35 145 4.31 0.68 4.31 146 3.43 0.83 3.43 147 4.20 0.82 4.20 148 4.11 0.77 4.11 149 3.87 0.79 3.87 150 3.94 0.95 3.94 151 4.72 0.97 4.72 152 4.79 0.81 4.79 153 4.03 0.84 4.03 154 4.13 0.78 4.13 155 3.83 0.91 3.83 156 4.45 0.88 4.45 157 4.29 0.91 4.29 158 4.46 0.93 4.46 159 4.54 1.01 4.54 160 4.89 0.89 4.89 161 4.33 0.94 4.33 162 4.53 1.07 4.53 163 5.17 0.90 5.17 164 4.34 0.90 4.34 165 4.30 1.01 4.30 166 4.82 0.97 4.82 167 4.62 0.99 4.62 168 4.73 0.85 4.73 169 4.04 1.06 4.04 170 5.00 1.03 5.00 171 4.88 1.04 4.88 172 4.90 0.98 4.90 173 4.59 0.94 4.59 174 4.39 0.92 4.39 175 4.32 1.11 4.32 176 5.19 0.98 5.19 MAR cm % MAR 0.82 130 3.58 0.78 0.77 131 3.44 0.71 0.79 132 3.63 0.73 0.80 133 3.11 0.64 0.79 134 3.27 0.64 0.76 135 3.19 0.71 0.80 136 3.00 0.63 0.84 137 3.13 0.67 0.77 138 3.29 0.73 0.79 139 3.21 0.69 0.75 140 3.40 0.70 0.82 141 4.01 0.85 0.81 142 3.77 0.81 0.73 143 3.29 0.65 0.78 144 3.23 0.63 0.78 145 3.18 0.64 0.63 146 3.29 0.64 0.80 147 3.18 0.70 0.79 148 3.12 0.66 0.78 149 3.08 0.67 0.86 150 2.93 0.64 0.99 151 3.15 0.71 0.97 152 3.31 0.79 0.83 153 3.38 0.84 0.88 154 3.47 0.81 0.75 155 3.35 0.76 0.84 156 3.40 0.77 0.83 157 3.25 0.70 0.86 158 3,26 0.77 0.92 159 3.37 0.83 0.99 160 3.15 0.76 0.87 161 3.30 0.80 0.92 162 3.45 0.82 1.05 163 3.44 0.83 0.86 164 3.28 0.79 0.84 165 3.46 0.79 0.88 166 3.53 0.89 0.84 167 2.61 0.68 0.87 168 3.49 0.84 0.78 169 3.37 0.72 0.90 170 3.21 0.61 0.86 171 3.05 0.44 0.86 172 3.22 0.47 0.82 173 3.18 0.65 0.81 174 3.31 0.75 0.82 175 3.47 0.79 0.91 176 3.39 0.75 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 204 cm % MAR % MAR cm % MAR 177 4.57 1.04 4.57 0.81 177 3.22 0.69 178 4.83 0.93 4.83 0.90 178 3.50 0.74 179 4.32 1.00 4.32 0.81 179 3.32 0.73 180 4.62 0.93 4.62 0.90 180 3.28 0.76 181 4.29 0.99 4.29 0.87 181 3.13 0.71 182 4.55 1.05 4.55 0.86 182 3.34 0.75 183 4.81 0.98 4.81 0.89 183 3.27 0.76 184 4.47 0.91 4.47 0.82 184 2.85 0.65 185 4.15 0,97 4.15 0.80 185 2.92 0.62 186 4.41 0.89 4.41 0.82 186 3.18 0.72 187 4.02 1.01 4.02 0.81 187 3.22 0.78 188 4.60 1.03 4.60 0.86 188 3.33 0.78 189 4.65 0.94 4.65 0.89 189 3.59 0.75 190 4.25 0.88 4.25 0.83 190 3.47 0.79 191 3.95 0.92 3.95 0.76 191 3.49 0.75 192 4.13 0.95 4.13 0.84 192 3.38 0.75 193 4.27 0.96 4.27 0.83 193 3.31 0.73 194 4.30 0.90 4.30 0.84 194 3.08 0.70 195 4.02 1.03 4.02 0.79 195 3.38 0.76 196 4.57 1.04 4.57 0.86 196 2.82 0.60 197 4.63 0.84 4.63 0.79 197 3.16 0.69 198 3.71 0.91 3.71 0.72 198 3.32 0.70 199 3.99 0.84 3.99 0.74 199 3.42 0.79 200 3.70 0.84 3.70 0.75 200 3.44 0.77 201 3.69 0.80 3.69 0.80 201 3.33 0.74 202 3.53 0.78 3.04 0.75 202 3.32 0.78 203 3.39 0.78 3.04 0.69 203 3.22 0.71 204 3.41 0.76 3.06 0.72 204 3.10 0.68 205 3.31 0.73 3.23 0.73 205 4.26 0.93 206 3.18 0.72 3.38 0.73 206 3.23 0.75 207 3.10 0.72 4.75 0.90 207 2.83 0.66 208 3.12 0.75 5.33 1.00 208 3.82 0.89 209 3.24 0.74 4.72 0.93 209 3.61 0.85 210 3.17 0.71 5.40 1.06 210 2.95 0.69 211 3.06 0.75 4.72 0.94 211 3.31 0.76 212 3.20 0.00 5.00 0.99 212 3.36 0.77 213 4.84 0.81 213 3.46 0.77 214 4.90 0.86 214 3.59 0.75 215 5.34 0.88 215 3.45 0.71 216 5.01 1.01 216 3.24 0.70 217 5.26 0.99 217 3.45 0.74 218 5.29 1.07 218 3.34 0.71 219 4.75 1.01 219 3.17 0.68 220 4.65 0.99 220 3.18 0.66 221 4.74 1.01 221 3.29 0.76 222 4.74 1.03 222 3.15 0.69 223 4.87 1.01 223 3.18 0.72 % MAR cm % MAR 4.43 0.89 224 3.21 0.69 4.41 0.88 225 3.22 0.71 4.74 0.94 226 3.52 0.83 5.05 1.00 227 3.19 0.75 5.00 0.99 228 3.33 0.81 4.85 0.92 229 3.55 0.83 4.51 0.90 230 3.35 0.72 4.70 0.93 231 3.35 0.75 5.10 1.04 232 3.39 0.72 4.68 0.90 233 3.22 0.66 4.38 0.89 234 3.17 0.70 4.64 0.93 235 3.22 0.71 4.54 0.91 236 2.97 0.69 4.57 0.90 237 2.99 0.70 4.71 0.92 238 2.97 0.67 239 3.26 0.76 240 3.35 0.79 241 3.50 0.86 242 3.18 0.77 243 3.30 0.80 244 3.34 0.78 245 3.42 0.77 246 3.34 0.73 247 3.35 0.76 248 3.22 0.72 249 3.15 0.68 250 3.16 0.73 251 3.28 0.77 252 3.22 0.77 253 3.31 0.80 254 2.90 0.67 255 3.49 0.79 256 3.38 0.78 257 3.27 0.78 258 3.01 0.72 259 3.34 0.75 260 3.38 0.75 261 3.33 0.79 262 3.29 0.77 263 3.41 0.76 264 3.40 0.77 265 3.44 0.81 266 3.49 0.78 267 3.39 0.78 268 3.38 0.75 269 3.44 0.77 270 3.52 0.80 cm 224 225 226 227 228 229 230 231 232 233 234 235 236 237 238 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 205 cm % MAR % cm % MAR 271 3.34 0.77 272 3.57 0.81 273 3.44 0.78 274 3.33 0.76 275 3.36 0.78 276 3.46 0.78 277 3.42 0.77 278 3.25 0.79 279 3.33 0.76 280 3.27 0.73 281 3.08 0.69 282 3.07 0.72 283 3.10 0.71 284 3.20 0.74 285 3.19 0.77 286 3.16 0.78 287 3.23 0.80 288 3.37 0.82 289 3.13 0.71 290 3.30 0.77 291 3.36 0.81 292 3.39 0.83 293 3.24 0.81 294 3.01 0.77 295 3.60 0.87 296 3.43 0.81 297 3.32 0.78 298 3.28 0.79 299 3.43 0.82 300 3.28 0.76 301 3.34 0.81 302 3.60 0.87 303 3.37 0.85 304 3.25 0.82 305 3.18 0.85 306 3.18 0.74 307 3.44 0.77 308 3.22 0.81 309 3.52 0.92 310 3.41 0.90 311 3.24 0.84 312 3.50 0.90 313 3.50 0.77 314 3.44 0.75 315 3.47 0.81 316 3.23 0.80 317 3.21 0.82 cm % MAR 318 3.28 0.83 319 3.07 0.77 320 3.10 0.73 321 3.06 0.76 322 3.86 0.95 323 3.09 0.80 324 2.58 0.66 325 2.92 0.76 326 3.22 0.82 327 3.16 0.83 328 2.99 0.75 329 3.19 0.77 330 3.15 0.70 331 2.90 0.61 332 2.82 0.60 333 2.88 0.67 334 3.43 0.86 335 3.51 0.88 336 2.97 0.71 337 3.18 0.76 338 3.04 0.75 339 2.84 0.72 340 3.38 0.85 341 3.05 0.75 342 3.16 0.80 343 2.95 0.74 344 3.31 0.84 345 2.82 0.72 346 2.79 0.70 347 2.76 0.68 348 3.09 0.67 349 2.92 0.63 350 2.61 0.57 351 2.88 0.68 352 3.20 0.81 353 2.81 0.67 354 2.99 0.65 355 2.96 0.65 356 3,05 0.67 357 2.76 0.66 358 3.19 0.78 359 2.87 0.68 360 2.93 0.70 361 3.07 0.73 362 3.31 0.81 363 3.14 0.71 364 3.03 0.67 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 206 cm % MAR % MAR cm % MAR 365 3.23 0.70 366 3.02 0.69 367 3.31 0.81 368 3.06 0.69 369 2.63 0.61 370 3.03 0.70 371 2.94 0.69 372 2.85 0.69 373 2.87 0.69 374 2.52 0.62 375 2.62 0.66 376 2.61 0.66 377 2.76 0.70 378 2.86 0.73 379 2.73 0.71 380 2.99 0.76 381 2.65 0.68 382 3.05 0.77 383 3.17 0.80 384 3.82 0.99 385 2.86 0.76 386 3.04 0.79 387 3.18 0.84 388 2.90 0.76 389 2.82 0.72 390 2.99 0.77 cm % MAR % MAR cm Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. /. MAR 207 Appendix I:Percentage and MAR of CaC03 in all cores (MAR Values in mg/cm2/year) Alfonso Basin Pescadero Basin CP CB NH01-15 NH01-26 cm % M A R % % M A R cm % M AR 1 11.4 1.108 X 15.11 1.89 1 5.5 1.13 2 9.8 0.969 X 10.65 1.30 2 5.84 1.135 3 7.2 0.724 X 8.78 1.01 3 5.19 0.93 4 6.2 0.634 X 6.43 0.74 4 4.52 0.758 5 8.6 0.893 9.27 5.52 0.64 5 4.24 0.739 6 4.1 0.433 9.46 6.37 0.71 6 4.79 0.794 7 3.6 0.386 11.29 9.77 1.06 7 5.28 0.885 8 6.2 0.676 12.33 9.63 1.03 8 4.75 0.794 9 6.7 0.742 13.36 9.78 1.07 9 4.34 0.674 10 10.3 1.158 13.07 7.92 0.88 10 4.31 0.693 1 1 9.8 1.119 12.57 7.51 0.82 1 1 4.94 0.863 12 9.8 1.136 15.09 5.71 0.81 12 4.22 0.959 13 7.8 0.918 12.65 5.76 0.80 13 4.08 0.878 14 9.3 1.111 8.80 4.25 0.51 14 4.68 0.961 15 9.8 1.188 7.76 7.72 0.92 15 4.1 0.863 16 11.8 1.452 8.88 8.10 0.95 16 4.37 0.887 17 10.8 1.349 9.78 12.63 1.48 17 2.77 0.535 18 8.7 1.102 16.01 11.30 1.28 18 1.91 0.349 19 10.8 1.388 16.85 8.90 0.94 19 2.38 0.427 20 10.2 1.33 11.11 10.83 1.14 20 1.79 0.282 21 11.4 1.507 7.50 11.01 1.18 21 1.85 0.306 22 16 2.124 7.50 11.60 1.25 22 2.06 0.36 23 5.2 0.693 16.93 10.96 1.17 23 2.04 0.341 24 1 0.134 15.79 10.02 1.06 24 2.16 0.38 25 2.6 0.349 14.12 10.67 1.14 25 2.85 0.509 26 2.1 0.283 12.44 11.30 1.17 26 3.05 0.531 27 6.2 0.84 8.92 12.15 1.19 27 2.21 0.384 28 2.1 0.285 6.04 11.11 1.22 28 1.52 0.269 29 5.3 0.723 10.97 12.33 1.31 29 1.96 0.359 30 9.5 1.302 13.09 12.61 1.34 30 1.49 0.266 31 6.8 0.935 9.49 10.81 1.21 31 2.02 0.374 32 5.8 0.801 5.49 10.82 1.19 32 2.2 0.395 33 5.7 0.79 5.43 13.40 1.52 33 1.97 0.357 34 7.8 1.085 12.65 10.66 1.24 34 2.08 0.376 35 8.3 1.159 14.66 8.51 0.94 35 1.92 0.328 36 11.3 1.584 12.42 9.44 1.01 36 1.29 0.248 37 8.3 1.168 10.23 11.65 1.31 37 1.76 0.321 38 9.3 1.314 9.19 9.66 1.02 38 2.12 0.375 39 11.3 1.602 9.64 16.08 1.73 39 2.79 0.475 40 11.4 1.623 9.80 18.10 2.12 40 2.93 0.506 41 10.3 1.472 11.90 13.11 1.48 41 2.9 0.468 42 7.7 1.104 12.18 9.23 0.99 42 2.92 0.558 43 5.2 0.748 13.38 9.27 1.06 43 2.92 0.494 44 10.8 1.56 14.57 11.79 1.35 44 3.12 0.576 45 7.2 1.044 17.45 13.12 1.49 45 3.68 0.674 46 4.6 0.669 16.47 11.41 1.25 46 3.79 0.672 47 6.2 0.906 9.14 9.28 1.04 47 4.3 0.821 48 3.1 0.454 10.12 9.43 1.02 48 3.38 0.674 49 2.6 0.383 12.81 10.28 1.19 49 2.06 0.419 50 2.1 0.31 12.99 12.69 1.40 50 2.94 0.589 51 2 0.296 21.13 12.24 1.45 51 3.17 0.588 52 3.6 0.535 15.01 11.17 1.38 52 2.93 0.549 53 4.7 0.702 10.48 9.46 1.26 53 3.46 0.627 Alfonso Basin Pescadero Basin CP CB NH01-15 NH01-26 cm % M A R % % M A R cm % M A R 54 5.6 0.839 10.77 10.19 1.26 54 2.909 0.57 55 4.6 0.692 7.40 11.70 1.43 55 2.701 0.48 56 6.7 1.011 10.26 12.72 1.69 56 3.712 0.75 57 8.7 1.317 8.71 10.05 1.28 57 3.88 0.72 58 8.7 1.322 6.52 8.76 1.03 58 3.409 0.6 59 9.2 1.403 5.37 12.95 1.60 59 2.806 0.52 60 10.3 1.576 6.04 11.82 1.54 60 1.54 0.3 61 8.4 1.29 5.94 14.55 1.95 61 0.601 0.12 62 7.9 1.217 5.84 11.07 1.48 62 0.627 0.13 63 3.1 0.479 6.35 13.50 1.81 63 0.572 0.11 64 7.3 1.133 6.42 9.68 1.26 64 1.102 0.21 65 7.3 1.136 5.70 13.60 1.59 65 2.164 0.36 66 7.7 1.203 5.81 11.12 1.35 66 2.96 0.52 67 7.2 1.129 7.83 9.71 1.20 67 3.239 0.53 68 10.3 1.62 7.74 7.57 0.97 68 1.183 0.23 69 12 1.894 8.27 5.62 0.72 69 3.611 0.69 70 9.3 1.473 7.97 5.71 0.71 70 4.052 0.78 71 15.4 2.447 8.43 7.04 0.89 71 4.236 0.84 72 6.7 1.068 7.25 8.11 1.06 72 3.104 0.63 73 3.5 0.56 8.64 8.52 1.16 73 2.919 0.6 74 2.1 0.337 9.10 6.79 0.84 74 2.789 0.54 75 5.7 0.918 9.33 9.13 1.18 75 2.705 0.51 76 10 1.615 10.06 11.61 1.51 76 2.291 0.44 77 15.5 2.512 9.45 9.65 1.22 77 1.68 0.31 78 8.4 1.366 8.59 11.51 1.59 78 1.067 0.2 79 5.7 0.93 7.72 10.92 1.46 79 0.776 0.14 80 4.7 0.769 4.96 9.63 1.25 80 0.99 0.17 81 4.1 0.673 8.19 10.46 1.39 81 1.007 0.18 82 7.2 1.186 8.39 8.58 1.09 82 1.099 0.18 83 6.7 1.107 6.94 12.19 1.51 83 0.798 0.15 84 9.8 1.625 12.31 7.58 1.01 84 0.861 0.17 85 11.3 1.88 13.21 13.08 1.68 85 0.792 0.14 86 1 1 1.836 17.79 13.84 1.89 86 1.237 0.23 87 12.4 2.076 25.01 9.58 1.35 87 1.444 0.24 88 8.3 1.394 11.38 7.36 1.06 88 1.321 0.26 89 6.7 1.129 14.30 9.76 1.36 89 1.287 0.23 90 11.9 2.011 17.24 7.62 1.05 90 0.736 0.16 91 7.8 1.322 19.91 8.86 0.91 91 0.712 0.14 92 4.7 0.799 23.70 16.37 1.76 92 1.275 0.23 93 5.7 0.972 14.10 13.15 1.89 93 2.658 0.51 94 10.4 1.78 17.22 6.72 0.93 94 3.302 0.55 95 10.3 1.768 15.12 11.63 1.73 95 3.243 0.58 96 10.2 1.757 15.17 12.31 1.65 96 3.042 0.6 97 14.9 2.574 15.21 14.25 1.92 97 1.858 0.37 98 18.2 3.154 15.47 18.55 2.62 98 1.492 0.3 99 22.9 3.98 16.65 16.77 2.47 99 1.47 0.31 100 17 2.964 16.61 8.90 1.31 100 1.334 0.27 101 10.3 1.801 19.73 8.60 1.24 101 2.651 0.5 102 11.5 2.017 15.40 9.49 1.40 102 2.185 0.41 103 10.9 1.918 16.73 10.34 1.47 103 2.767 0.6 104 14.1 2.488 18.21 9.53 1.41 104 3.061 0.65 105 17.1 3.027 10.88 8.75 1.24 105 2.432 0.48 106 13.1 2.326 16.04 12.93 1.89 106 1.885 0.37 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 208 cm % M A R % % M A R 107 27.5 4.897 17.39 13.01 2.01 108 17.5 3.126 12.34 10.17 1.45 109 16.8 3.01 16.08 11.51 1.63 110 18.8 3.378 18.26 13.28 2.00 111 25.4 4.577 26.21 13.22 1.91 112 22.3 4.031 24.64 12.65 1.92 113 14.2 2.574 21.16 15.93 2.31 114 16 2.909 16.40 12.06 1.81 115 23.5 4.285 11.64 12.33 1.78 116 20 3.658 10.20 12.07 1.82 117 17.6 3.228 9.58 18.93 2.84 118 11.7 2.152 10.97 17.92 2.75 119 13.3 2.454 10.83 10.96 1.58 120 21.4 3.959 17.22 17.79 2.71 121 19.8 3.674 24.82 19.25 3.05 122 15.2 2.828 21.74 20.43 3.25 123 18.3 3.415 24.08 28.19 4.16 124 14.5 2,714 19.11 29.49 5.38 125 14 2.627 12.04 25.66 4.75 126 8.8 1.656 17.10 19.95 3.49 127 15.1 2.85 21.07 9.70 1.69 128 14.2 2.688 17.20 11.77 2.01 129 16.1 3.056 10.54 11.22 1.95 130 14 2.665 11.13 11.25 1.93 131 16.3 3.111 17.41 13.50 2.39 132 1 1 2.106 23.69 13.54 2.44 133 1 1 2.111 20.43 11.76 2.02 134 13 2.502 17.86 14.14 2.43 135 10.3 1.988 14.60 18.32 3.46 136 7.4 1.432 12.46 15.68 2.92 137 1 1 2.135 13.22 20.61 3.56 138 15 2.919 17.48 22.26 4.02 139 13.6 2.654 17.03 23.93 4.46 140 15.1 2.955 17.60 19.94 3.80 141 13.3 2.61 14.50 13.66 2.50 142 10 1.967 11.62 10.47 1.94 143 1 1 2.17 11.95 15.53 2.91 144 13.6 2.69 10.08 28.06 5.00 145 14.8 2.936 8.87 29.75 5.38 146 10.1 2.009 9.88 31.18 5.75 147 12.3 2.453 14.91 21.02 4.00 148 13.8 2.759 12.60 21.09 4.07 149 10.3 2.065 13.83 18.64 3.76 150 10.4 2.091 15.05 13.03 2.86 151 12 2.419 10.34 10.03 2.10 152 8.5 1.718 9.10 17.60 3.58 153 7.7 1.56 13.32 24.79 5.12 154 8.7 1.767 10.46 21.13 4.50 155 11.3 2.302 13.06 20.07 3.92 156 12.8 2.614 12.57 20.74 3.91 157 10 2.047 11.91 16.87 3.25 158 8.7 1.786 8.02 14.88 2.87 159 12.5 2.573 10.07 11.78 2.38 160 11.1 2.29 13.12 10.73 2.16 161 11.3 2.338 18.38 18.02 3.64 162 11.7 2.427 19.32 21.48 4.35 163 16.2 3.369 12.92 18.89 3.82 1164 12.7 2.648 9.29 19.34 3.85 cm % M A R cm % M A R 107 1.85 0.369 165 10.3 2.153 108 1.29 0.245 166 6.6 1.383 109 1.57 0.292 167 6.7 1.408 110 1.61 0.299 168 12.2 2.569 111 2.01 0.381 169 16.8 3.547 112 2.56 0.453 170 10.2 2.159 113 3.07 0.569 171 11.2 2.377 114 3.19 0.583 172 15.2 3.234 115 3.1 0.587 173 11.9 2.538 116 3.06 0.606 174 11.4 2.437 117 2.8 0.619 175 12.7 2.722 118 3.14 0.641 176 10.8 2.321 119 2.71 0.563 177 7.5 1.616 120 2.77 0.634 178 7.4 1.598 121 3.63 0.772 179 4 0.866 122 3.48 0.744 180 9.6 2.083 123 3.52 0.709 181 9.1 1.98 124 4.31 0.899 182 12 2.617 125 3.11 0.613 183 9.2 2.011 126 2.48 0.538 184 11.7 2.564 127 2.47 0.502 185 10.9 2.395 128 2.44 0.502 186 8.7 1.916 129 2.63 0.56 187 8.3 1.832 130 2.33 0.508 188 6.5 1.438 131 2.07 0.427 189 6.4 1.42 132 1.88 0.378 190 7.4 1.645 133 2.28 0.473 191 16.5 3.678 134 2.95 0.573 192 15.4 3.441 135 3.76 0.839 193 9.2 2.06 136 4.09 0.86 194 1 1 2.469 137 4.7 1.006 195 7.7 1.733 138 5.99 1.33 196 11.3 2.549 139 5.29 1.139 197 11.1 2.51 140 5.14 1.063 198 13.5 3.059 141 4.34 0.918 199 15.1 3.43 142 3.6 0.776 200 5.8 1.321 143 2.63 0.518 201 13 2.967 144 2.38 0.467 202 22.2 5.078 145 2.53 0.511 203 19.7 4.517 146 2.85 0.555 204 23.5 5.401 147 2.77 0.605 205 17.4 4.008 148 2.92 0.615 206 17.3 3.994 149 2.83 0.616 207 18.3 4.235 150 2.57 0.561 208 17 3.943 151 2.09 0.474 209 22.9 5.324 152 2.34 0.558 210 18.8 4.381 153 2.77 0.686 211 16.3 3.807 154 2.67 0.624 212 13.6 3.184 155 3.28 0.749 213 156 3.25 0.735 214 157 4.15 0.888 215 158 3.25 0.765 216 159 2.74 0.673 217 160 3.02 0.732 218 161 2.61 0.632 219 162 2.24 0.535 220 163 1.55 0.374 221 164 0 0 222 % % M AR cm % M A R 12.65 19.54 3.81 165 0 0 12.52 18.29 3.35 166 0 0 12.93 12.16 2.22 167 0 0 13.33 10.71 1.98 168 0 0 16.15 13.17 2.55 169 0 0 13.40 11.48 2.07 170 3.766 0.72 10.59 13.79 2.42 171 2.757 0.4 8.19 13.76 2.41 172 1.508 0.22 12.08 13.07 2.34 173 0.42 0.09 15.96 18.30 3.39 174 0.131 0.03 10.24 17.44 3.33 175 0.396 0.09 13.13 11.84 2.09 176 1.467 0.33 12.49 20.68 3.68 177 1.92 0.41 10.30 18.77 3.52 178 2.71 0.57 13.73 18.90 3.52 179 2.577 0.57 11.50 18.59 3.62 180 2.396 0.56 11.50 15.23 3.08 181 2.073 0.47 10.82 12.35 2.34 182 2.037 0.46 11.14 9.72 1.80 183 1.39 0.32 11.25 14.01 2.56 184 1.881 0.43 11.36 12.24 2.36 185 2.824 0.6 8.55 18.15 3.36 186 2.845 0.64 8.51 21.00 4.22 187 3.02 0.73 7.50 10.69 2.00 188 4.394 1.03 10.93 13.17 2.52 189 3.653 0.76 16.86 22.73 4.41 190 2.715 0.62 14.77 15.18 2.94 191 2.352 0.51 13.63 11.43 2.32 192 2.134 0.47 11.92 16.56 3.21 193 2.03 0.45 10.48 15.53 3.03 194 1.752 0.4 16.12 23.42 4.60 195 1.924 0.43 20.12 11.39 2.13 196 2.479 0.53 15.47 10.21 1.74 197 2.934 0.64 19.88 9.94 1.93 198 3.588 0.75 23.52 17.97 3.31 199 4.595 1.07 25.40 15.81 3.22 200 5.45 1.21 17.61 15.36 3.35 201 3.656 0.82 18.16 14.55 3.57 202 2.769 0.65 18.70 13.92 3.18 203 2.268 0.5 18.03 13.10 3.09 204 2.134 0.47 22.12 13.15 2.96 205 2.784 0.61 19.85 16.98 3.67 206 2.545 0.59 15.43 11.44 2.17 207 2.48 0.58 14.81 5.76 1.08 209 2.456 0.57 11.21 6.55 1.28 210 2.205 0.52 7.41 8.37 1.65 211 0.989 0.23 6.68 9.40 1.87 212 0.244 0.06 12.50 2.48 213 0.161 0.04 14.33 2.40 214 0.121 0.03 7.95 1.39 215 0.378 0.08 9.20 1.53 216 0.301 0.06 10.61 2.13 217 0.25 0.05 8.01 1.50 218 0.15 0.03 12.83 2.60 219 0.336 0.07 16.07 3.42 220 0.977 0.21 14.92 3.18 221 1.188 0.25 12.75 2.72 222 1.436 0.33 12.58 2.73 223 2.641 0.58 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 209 cm % M A R % % M A R cm % M A R 223 12.92 2.67 224 2.78 0.629 224 13.84 2.79 225 2.24 0.482 225 12.56 2.49 226 1.88 0.418 226 12.11 2.39 227 1.08 0.253 227 9.32 1.85 228 0.62 0.146 228 13.99 2.77 229 0.36 0.088 229 18.90 3.57 230 1 0.234 230 16.37 3.26 231 2.13 0.456 231 12.32 2.45 232 3.37 0.758 232 10.55 2.15 233 3.58 0.756 233 15.65 3.00 234 3.43 0.699 234 14.71 2.98 235 3.3 0.733 235 12.51 2.51 236 3.58 0.792 236 10.82 2.16 237 2.98 0.691 237 17.67 3.50 238 2.86 0.674 238 13.49 2.64 239 3.18 0.714 239 17.17 240 3.03 0.706 240 17.28 241 2.65 0.625 241 17.22 242 2.83 0.693 242 17.32 243 2.44 0.588 243 17.24 244 3.62 0.88 244 17.25 245 4.85 1.139 245 17.28 246 5.36 1.203 246 17.34 247 4.39 0.956 247 17.27 248 4.06 0.92 248 17.14 249 4.09 0.916 249 17.62 250 4.34 0.941 250 17.42 251 4.69 1.086 251 17.33 253 5.87 1.387 252 17.42 254 4.1 0.98 253 17.63 255 4.59 1.108 254 17.59 256 3.52 0.815 255 17.52 257 3.23 0.736 256 17.35 258 3.41 0.788 257 17.42 259 3.99 0.949 258 17.47 260 3.04 0.729 259 17.40 261 2.45 0.551 260 17.50 262 2.68 0.597 261 17.37 263 2.8 0.667 262 17.35 264 2.67 0.624 263 17.29 265 2.95 0.659 264 17.43 266 3.26 0.736 265 17.35 267 3.02 0.714 266 17.35 268 3.24 0.728 267 17.42 269 5.18 1.191 268 17.49 270 5.28 1.177 269 17.65 271 4.1 0.923 270 18.60 272 2.89 0.66 271 18.19 273 3.16 0.73 272 14.55 274 3.04 0.692 273 13.92 275 2.83 0.646 274 13.10 276 2.79 0.64 275 13.15 277 3.73 0.862 276 16.98 278 3.96 0.891 277 11.44 279 4.05 0.91 278 5.76 280 3.82 0.928 279 6.55 281 2.37 0.542 280 8.37 282 2.68 0.595 cm % M A R % % M AR cm % M A R 281 9.40 283 3.519 0.79 282 12.50 284 3.341 0.78 283 14.33 285 2.285 0.52 284 7.95 286 1.815 0.42 285 9.20 287 1.652 0.4 286 10.61 288 2.388 0.59 287 8.01 289 2.765 0.68 288 12.83 290 3.289 0.8 289 16.07 291 3.639 0.83 290 14.92 292 2.942 0.69 291 12.75 293 3.264 0.79 292 12.58 294 2.82 0.69 293 12.92 295 2.386 0.59 294 13.84 296 1.242 0.32 295 12.56 297 0.749 0.18 296 12.11 298 1.824 0.43 297 9.32 299 3.201 0.75 298 13.99 300 3.672 0.88 299 18.90 301 3.094 0.74 300 16.37 302 0.981 0.23 301 12.32 303 0 0 302 10.55 304 0.111 0.03 303 15.65 305 2.775 0.7 304 14.71 306 2.283 0.57 305 12.51 307 1.054 0.28 306 10.82 308 1.134 0.26 307 17.67 309 0.55 0.12 308 13.49 310 0.495 0.12 311 2.12 0.55 312 2.432 0.64 313 2.276 0.59 314 2.092 0.54 315 2.673 0.58 316 3.727 0.82 317 3.975 0.93 318 4.189 1.04 319 4.242 1.08 320 3.023 0.77 321 4.508 1.13 322 5.275 1.25 323 2.673 0.66 324 0.693 0.17 325 2.631 0.68 326 0.631 0.16 327 0.508 0.13 328 0.061 0.02 329 0.434 0.11 330 0.714 0.18 331 0.465 0.11 332 1.461 0.32 333 2.812 0.59 334 3.823 0.82 335 1.216 0.28 336 0.092 0.02 337 0.669 0.17 338 3.115 0.75 339 0.139 0.03 340 0.097 0.02 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 2 1 0 cm % MAR % % M A R cm % M A R 341 0.13 0.034 342 0.15 0.038 343 1.4 0.343 344 0.68 0.17 345 1.54 0.387 346 2.72 0.69 347 23 5.926 348 12.9 3.224 349 7.21 1.768 350 0.74 0.161 351 0.21 0.045 352 14.1 3.102 353 8.46 1.994 354 4.55 1.155 355 2.63 0.623 356 2.32 0.508 357 2.07 0.452 358 1.08 0.238 359 1 0.24 360 0.89 0.215 361 1.16 0.277 362 1.58 0.375 363 1.09 0.261 364 0.6 0.147 365 1.04 0.236 366 3.16 0.703 367 2.51 0.543 368 0.8 0.183 369 1.41 0.347 370 13.4 3.003 371 9.21 2.145 372 0.54 0.125 373 0 0.001 374 0.09 0.021 375 0.49 0.117 376 0.78 0.19 377 1.44 0.361 378 0.93 0.234 379 0.78 0.196 380 1.62 0.415 381 2.8 0.728 382 4.02 1.016 383 3.22 0.822 384 1.05 0.265 385 0.02 0.005 386 0.95 0.246 387 1.34 0.355 388 0.19 0.05 389 1.54 0.408 390 1.63 0.426 391 2.43 0.618 392 1.81 0.466 cm % MAR % % MAR cm ■ Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. % MAR Appendix J: Cycles obtained with MTM Spectral Analysis in ail cores Productivity Proxies Carb CB 2218 Carb CP carb15 carb26 TOC15 TOC26 2176 Opal15 3176 0pal26 1407 1341 1985 1281 1609 1510 1633+/-352 794 804 863 82S+/-44 484 625 381 409 407 391*7-14 363 351 333 303 289 ____ 257 261 242 [ 252+/-10 207 193 197 180 192 198+/-9 156 163 169 131 138 132 139 138 138*1-7 122 121 99 100 105 109 109 102 107 112 105*7-7 92 88 87 88 88 91 92 90+/-3 78 76 81 78 71 72 73172+/-1 64 65 60 65 58 58 55 54 56 55 54 55*7-1 Rainfall P roxies Med 15 Mean 15 SO 15 Med 26 51 52 Mean 26 SD 26 Terr 15 3452 49 Terr 26 1620 1557 1574 1510 1565*7-55 831 1014 533 497 490 533 I512+/-22 400 359 347 347 351 1 353+7-5 213 249 258 269 197 191 192 201 1196+7-5 149 166 ....... 134 133 132 132+7-1 121 122 112 100 102 104 101 99 103 105 102*7-3 85 88 87 86 90] 83+7-3 79 78 80 79+71 72 72 731 72+71 63 65 65 64 66 62 681 65+7-3 58 57 53 54 53 51 51 501 52+7-2 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission.

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Barnacles as mudstickers? The paleobiology, paleoecology, and stratigraphic significance of Tamiosoma gregaria in the Pancho Rico Formation, Salinas Valley, California

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Early Jurassic reef eclipse: Paleoecology and sclerochronology of the "Lithiotis" facies bivalves

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Early Diagenesis In Southern California Continental Borderland Sediments

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Integrated geochemical and hydrodynamic modeling of San Diego Bay, California

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Grain-size and Fourier grain-shape sorting of ooids from the Lee Stocking Island area, Exuma Cays, Bahamas

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Fractionation of nitrogen isotopes during early diagenesis

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Investigation into the tectonic significance of the along strike variations of the Peninsular Ranges batholith, southern and Baja California

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Helicoplacoid echinoderms: Paleoecology of Cambrian soft substrate immobile suspension feeders

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A real-time debris prediction model (USCDPM) incorporating wildfire and subsequent storm events

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Synoptic Surf Zone Sedimentation Patterns

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Analysis of the effect of varying port spacing on initial dilution for a multiport outfall diffuser

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Petrology And Depositional History Of Late-Precambrian - Cambrian Quartzites In The Eastern Mojave Desert, Southeastern California

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Biotic recovery from the end-Permian mass extinction: Analysis of biofabric trends in the Lower Triassic Virgin Limestone, southern Nevada

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A phylogenetic analysis of oological characters: A case study of saurischian dinosaur relationships and avian evolution

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Characterization of geochemical and lithologic variations in Milankovitch cycles: Green River Formation, Wyoming

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A proxy for reconstructing histories of carbon oxidation in the Northeast Pacific using the carbon isotopic composition of benthic foraminifera

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A geochemical and hydrological assessment of groundwater in the Portuguese Bend landslide, California

Asset Metadata

Creator Gonzalez-Yajimovich, Oscar Efrain (author)

Core Title Holocene sedimentation in the southern Gulf of California and its climatic implications

School Graduate School

Degree Doctor of Philosophy

Degree Program Geological Sciences

Publisher University of Southern California (original), University of Southern California. Libraries (digital)

Tag Geology,OAI-PMH Harvest

Language English

Contributor Digitized by ProQuest (provenance)

Advisor Douglas, Robert (committee chair), Gorsline, Donn (committee chair), Corsetti, Frank (committee member), Lee, Jiin-Jen (committee member), Sanchez, Enrique Nava (committee member)

Permanent Link (DOI) https://doi.org/10.25549/usctheses-c16-403382

Unique identifier UC11340785

Identifier 3145204.pdf (filename),usctheses-c16-403382 (legacy record id)

Legacy Identifier 3145204.pdf

Dmrecord 403382

Document Type Dissertation

Rights Gonzalez-Yajimovich, Oscar Efrain

Type texts

Source University of Southern California (contributing entity), University of Southern California Dissertations and Theses (collection)

Access Conditions The author retains rights to his/her dissertation, thesis or other graduate work according to U.S. copyright law. Electronic access is being provided by the USC Libraries in agreement with the au...

Repository Name University of Southern California Digital Library

Repository Location USC Digital Library, University of Southern California, University Park Campus, Los Angeles, California 90089, USA