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Thorium-230 normalized particle flux and sediment focusing in the Panama Basin region during the last.. Calvert, Stephen E. 2012

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Thorium-230 normalized particle flux and sediment focusing in the Panama Basin region during the last 30,000 years S. S. Kienast,1 M. Kienast,1 A. C. Mix,2 S. E. Calvert,3 and R. François3 Received 9 August 2006; revised 27 November 2006; accepted 5 December 2006; published 16 May 2007. [1] Application of the 230Th normalization method to estimate sediment burial fluxes in six cores from the eastern equatorial Pacific (EEP) reveals that bulk sediment and organic carbon fluxes display a coherent regional pattern during the Holocene that is consistent with modern oceanographic conditions, in contrast with estimates of bulk mass accumulation rates (MARs) derived from core chronologies. Two nearby sites (less than 10 km apart), which have different MARs, show nearly identical 230Th-normalized bulk fluxes. Focusing factors derived from the 230Th data at the foot of the Carnegie Ridge in the Panama Basin are >2 in the Holocene, implying that lateral sediment addition is significant in this part of the basin. New geochemical data and existing literature provide evidence for a hydrothermal source of sediment in the southern part of the Panama Basin and for downslope transport from the top of the Carnegie Ridge. The compilation of core records suggests that sediment focusing is spatially and temporally variable in the EEP. During oxygen isotope stage 2 (OIS 2, from 13–27 ka BP), focusing appears even higher compared to the Holocene at most sites, similar to earlier findings in the eastern and central equatorial Pacific. The magnitude of the glacial increase in focusing factors, however, is strongly dependent on the accuracy of age models. We offer two possible explanations for the increase in glacial focusing compared to the Holocene. The first one is that the apparent increase in lateral sediment redistribution is partly or even largely an artifact of insufficient age control in the EEP, while the second explanation, which assumes that the observed increase is real, involves enhanced deep sea tidal current flow during periods of low sea level stand. Citation: Kienast, S. S., M. Kienast, A. C. Mix, S. E. Calvert, and R. François (2007), Thorium-230 normalized particle flux and sediment focusing in the Panama Basin region during the last 30,000 years, Paleoceanography, 22, PA2213, doi:10.1029/2006PA001357. 1. Introduction [2] Upwelling of subsurface waters in the eastern equa- torial Pacific (EEP) results in elevated levels of primary production and particle export. Despite intensive research over the last several decades to reconstruct past variations in productivity and particle flux from surface waters to the seafloor, the interpretation of the sedimentary record in the EEP remains highly controversial (see Loubere [1999] and Paytan et al. [2004] for recent reviews). Linear sedimenta- tion rates calculated from core chronology often indicate higher mass accumulation of sedimentary material during the Last Glacial Maximum (LGM), which has been taken to imply higher vertical fluxes of biogenic sediment and higher productivity during this time interval [e.g., Sarnthein and Winn, 1988; Paytan et al., 1996; Lyle et al., 2002]. In contrast, ‘‘constant flux’’ tracers such as 230Th and extra- terrestrial 3He indicate that the vertical rain rates of partic- ulate biogenic material changed little or even decreased during the LGM [Marcantonio et al., 1996, 2001; Paytan et al., 1996; Higgins et al., 1999, 2002; Loubere et al., 2004; Kienast et al., 2006; Bradtmiller et al., 2006]. A similar discrepancy exists between different reconstructions of past aeolian dust fluxes to the central equatorial Pacific. While calculations based on linear sedimentation rates yield no consistent relationship between dust fluxes and glacial- interglacial stages [Murray et al., 1995], recent 230Th- normalized data suggest that dust fluxes were systematically higher during cold periods [Anderson et al., 2006]. [3] Studies using constant flux tracers invoke lateral redistribution of sediment on the seafloor to explain changes in sediment mass accumulation rates. Redistribution of recently deposited material (i.e., syndepositional redistribu- tion) from zones of sediment winnowing to zones to sediment focusing can significantly affect accumulation rates without impairing the stratigraphy or chronology of the sedimentary sequence and can thus be easily overlooked [François et al., 2004]. This process now appears much more common in the ocean than previously thought [e.g., Mollenhauer et al., 2003, 2005; François et al., 2004, and references therein; Mitchell and Lyle, 2005; Kienast et al., 2005], and failing to take it into account could obviously lead to significant errors if mass accumulation rates are used to evaluate past changes in the vertical rain rate of particles from overlying surface waters. PALEOCEANOGRAPHY, VOL. 22, PA2213, doi:10.1029/2006PA001357, 2007 1Department of Oceanography, Dalhousie University, Halifax, Nova Scotia, Canada. 2College of Oceanic and Atmospheric Sciences, Oregon State University, Corvallis, USA. 3Department of Earth and Ocean Sciences, University of British Columbia, Vancouver, Canada. Copyright 2007 by the American Geophysical Union. 0883-8305/07/2006PA001357 PA2213 1 of 19 [4] Normalization to the activity of the radioisotope 230Th has been proposed as a means to more accurately determine the vertical particle flux originating from surface waters [Bacon, 1984]. This approach relies on the assumption that the flux of 230Th to the seafloor approximates its rate of production by radioactive decay of 234U. Since it was first proposed, 230Th normalization is increasingly being used and its underlying assumptions are being tested and refined (see François et al. [2004], Henderson and Anderson [2003], and François et al. [2007], for recent reviews). Model simulations [e.g., Henderson et al., 1999; Marchal et al., 2000] and sediment trap observations [e.g., Yu et al., 2001, Scholten et al., 2005] confirm that the flux of scavenged 230Th to the seafloor is within 30% of its rate of production over most areas of the ocean. Laboratory experiments reveal that while 230Th has different affinities for different particle types (clay, biogenic opal, manganese oxide, and carbonate), all particle types strongly scavenge 230Th [Geibert and Usbeck, 2004]. [5] Using seismic data, Lyle et al. [2005] have recently questioned the validity of the interpretation of 230Th- normalized fluxes in the EEP, arguing that 230Th normali- zation grossly overestimates sediment redistribution. Here, we present new 230Th and compositional data from 4 cores from the Panama Basin region (Figure 1 and Table 1). We also revisit sites Y69-71 [Loubere et al., 2004; Lyle et al., 2005] and P7 [Pedersen et al., 1988; Yang et al., 1995] from the Panama Basin. Our results further validate the 230Th normalization method by showing that (1) 230Th-normalized fluxes of bulk sediment and organic carbon during the Holocene are regionally consistent with present-day sea surface conditions in the EEP, (2) two nearby sites with different sediment mass accumulation rates produce nearly identical 230Th-normalized bulk fluxes, and (3) the differ- ence in focusing factors derived from 230Th accumulation rates at these two sites is consistent with the difference in sediment accumulation rates estimated from seismic data [Lyle et al., 2005]. During the last glacial period (oxygen isotope stage 2, or OIS 2 from 13–27 ka BP), sediment redistribution appears to have been more intense, and we submit two possible explanations for this observation. 2. Core Sites and Oceanographic Setting [6] Cores ME0005-24JC and Y69-71 were recovered within 10 km of each other from an area of abyssal hills just to the north of the Carnegie Ridge (Figure 1 and Table 1). ME0005-24JC is located 200 m deeper than core Y69-71 in an abyssal valley [Mix et al., 2003], whereas Y69-71 was recovered midslope on an adjacent abyssal hill to the north, farther away from the Carnegie Ridge [see Lyle et al., 2005, Figure 1]. Core ME0005-24JC served as a site survey core for ODP Site 1240, which was subsequently drilled at this location. Core P7 was raised several hundred kilometers to the northeast from an area of relatively low Figure 1. Core sites used in this study. Bathymetry from Smith and Sandwell [1997], (http:// topex.ucsd.edu/marine_topo/mar_topo.html). Table 1. Cores Used in This Study Core ID Water Depth, m Longitude Latitude ME0005-24JC 2941 8627.7880W 001.3020N Y69-71P 2740 86290W 0060N P7 3085 8359.180W 236.260N ME0005-27JC 2203 8247.200W 151.2010S TR163-31P 3209 83.95 W 3.60 S TR163-19P 2348 9057.10W 215.50N PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 2 of 19 PA2213 relief. Core ME0005-27JC was raised on the southern flank of the Carnegie Ridge at 2203 m water depth (wd), from a bench that gently slopes to the south, approximately 20 km south of the main scarp of the Carnegie Ridge. ODP Site 1238 was subsequently drilled at this location. Further to the south, core TR163-31P was recovered from 3209 m wd. Finally, core TR163-19P was raised from 2348 m wd on the outer flank of the Cocos Ridge, which forms the western boundary of the Panama Basin. [7] The surface waters in the Panama Basin region are influenced by wind-driven upwelling of water from the equatorial undercurrent (EUC). Off Peru, nutrient-rich water originating from the deeper parts of EUC stimulates inten- sive production in the equatorial cold tongue as it recircu- lates into the south equatorial current [Toggweiler et al., 1991; Toggweiler and Carson, 1995; Dugdale et al., 2002]. Core sites TR163-31P and ME0005-27JC are affected most by these highly productive waters. Further northwest, cores ME0005-24JC and Y69-71 are situated within the equato- rial divergence zone, whereas cores P7 and TR163-19P are located at the northern boundary of the equatorial upwelling zone. The cores span a gradient in biological productivity with higher values (200 gC/m2/year) observed at sites TR163-31P and ME0005-27JC close to the Peru upwelling and lower values (140 gC/m2/yr) at sites P7 and TR163-19P at the northern limit of the shallow equatorial upwelling zone [Antoine et al., 1996]. 3. Experimental Section 3.1. Analytical Methods [8] Total 230Th, 232Th and 238U activities were determined at the Woods Hole Oceanographic Institution (WHOI) and the University of British Columbia (UBC) by isotope dilution on an inductively coupled plasma mass spectrometer (ICP-MS) following total acid digestion of sediment samples equilibrated with 229Th and 236U spikes. Details and principles of the procedure can be found in the work of Choi et al. [2001] and François et al. [2004]. Total 230Th data for core Y69-71 are from Loubere et al. [2004] and P. Loubere (personal communication, 2005) but multi- plied by 0.85 to correct for a standardization error at the time of measurement. For core P7, excess and decay corrected 230Th data were taken directly from Yang et al. [1995]. [9] Organic carbon (Corg) contents of coresME0005-24JC, ME0005-27JC, TR163-19P and TR163-31P were obtained at UBC by determining total C by combustion gas chroma- tography and subtracting carbonate carbon values deter- mined by coulometry [Calvert et al., 1993]. Carbonate (CaCO3) values were obtained from the coulometric CO2 determinations assuming no other carbonate-bearing phase was present. Precisions were ±3% of the reported values. For core Y69-71, Corg and CaCO3 values are taken from Lyle et al. [2002]; they were determined at Oregon State University (OSU) by the acidification/wet oxidation tech- nique described by Weliky et al. [1983] with modifications described by Lyle et al. [2002]. Organic carbon values of core P7 are taken from Pedersen et al. [1988]. [10] Biogenic opal (Siopal) of core ME0005-24JC was determined at UBC by extraction of silica from 20 mg subsamples by a 2M Na2CO3 solution at 85C for 5 hours. Dissolved silica concentrations in the extract were deter- mined by molybdenum blue spectrophotometry [Mortlock and Froelich, 1989]. Precision was ±4.3% (1s). Biogenic opal of core Y69-71 is taken from Lyle et al. [2002] and was obtained by determining Na2CO3-soluble Si by atomic absorption spectrophotometry [Lyle et al., 2002, 1988]. [11] Total Iron, Al, Mg, Si, and Mn contents of core ME0005-24JC were determined by ICP-OES analysis of subsamples fused in LiBO2 and redissolved in dilute HNO3. Accuracy was controlled by analyzing a wide range of international rock standards, and precisions were better than ±2%. Nonbiogenic Si in this core was derived by subtract- ing opaline Si (determined by alkaline extraction) from total Si (determined by ICP-OES). [12] Radiocarbon dates are based on accelerator mass spectrometry (AMS) of hand-picked N. dutertrei specimens and bulk carbonate samples and were carried out at the National Ocean Science Accelerator Mass Spectrometry Facility (NOSAMS) using standard procedures. 3.2. Core Chronologies [13] The accuracy of both mass accumulation rates (MARs) and focusing factors is strongly dependent on the availability of reliable core chronologies. A significant part of this work is thus dedicated to the presentation and discussion of age models and their effect on focusing factors and MARs. 3.2.1. Y69-71 [14] A new chronology for this core is presented here which is based on correlating the new high-resolution benthic d18O record (not shown) to core MD95-2042 off Portugal, which has been matched to the GRIP ice core record [Shackleton et al., 2000]. This tuning is confirmed by 8 14C dates obtained on N. dutertrei and bulk carbonate (Table 2 and Figure 2). Radiocarbon ages were calibrated to calendar years using the software CALIB 5.0.2 (Stuiver and Reimer [1993]; deltaR = 167 ± 106 years), except for the oldest 14C date, which was calibrated using the radiocarbon calibration of Fairbanks et al. [2005]. The new age model results in age assignments which are up to 2000 years older before 22 ka BP compared to the age model used in Loubere et al. [2004], which was based on the previous low-resolution d18O record and its correlation to SPECMAP (Figure 2). The differences in age models and their effects on focusing factors and MARs are discussed in section 4.3. 3.2.2. ME0005-24JC [15] The age model for core ME0005-24JC is based on correlating its carbonate record to that of core Y69-71 [see Lyle et al. 2005, Figure 2]. The resulting age model agrees well with 3 reservoir corrected (deltaR = 167 ± 106 years) and calibrated 14C dates on N. dutertrei during the degla- ciation, but gives a significantly older age assignment than a radiocarbon-based age point during the glacial period (Figure 2 and Table 2). Whereas we use the carbonate based stratigraphy for the main part of this contribution, we also discuss MARs and focusing factors that result from a radiocarbon based age model (section 4.3). Note that the PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 3 of 19 PA2213 radiocarbon age model requires linear extrapolation from the oldest 14C age fix point (at 20 ka) to the base of stage 2 at 27 ka. For the core top in the radiocarbon model, we adopted the age assignment derived from the correlated age model. 3.2.3. ME0005-27JC [16] The age model for core ME0005-27JC is based on 4 radiocarbon dates on N. dutertrei (Table 2), which were corrected for reservoir effects (deltaR = 167 ± 106 years) and then calibrated to calendar ages using CALIB 5.0.1, except for the oldest age, which was calibrated using the radiocarbon calibration compilation of Fairbanks et al. [2005]. Preliminary benthic d18O data (not shown) confirm this stratigraphy. 3.2.4. P7 [17] The age model of core P7 is taken from Pedersen et al. [1988] and Yang et al. [1995] and is based on 8 radio- carbon dates. 3.2.5. TR163-19P [18] The age model for TR163-19P is based on planktonic d18O [Lea et al., 2000] augmented by 2 radiocarbon measurements from the deglacial section of the core [Spero and Lea, 2002]. 3.2.6. TR163-31P [19] An age model for core TR163-31P based on a benthic d18O record and its correlation to SPECMAP was presented by Martin et al. [2002]. More recently, however, Skinner and Shackleton [2005] suggested that the postgla- cial benthic d18O rise in the EEP lagged the global gla- cioeustatic d18O component by 2 ka because of local hydrographic effects in the deep Pacific. Skinner and Shackleton [2005] base their findings on tight radiocarbon control on Kasten core TR163-31B, the companion core of TR163-31P used in this study. We thus present MARs and focusing factors based on the original stratigraphy [Martin et al., 2002] but also investigate the ‘‘Skinner effect’’ by subtracting 2 ka from core depths corresponding to the benthic d18O rise in TR163-31P. Figure 2. Depth-age relationships of core Y69-71 based on the new stratigraphy used here (thick dashed line) as well as the previously used age model (thin dashed line, Loubere et al. [2004]) and of core ME0005-24JC (thick solid line). Open symbols are calibrated 14C dates (Table 2). Table 2. Radiocarbon Data of Cores ME0005-24JC, -27JC and Y69-71P Core Depth, cm 14C Age, years Calendar Age,a years Laboratory Number Reference ME0005-24JC N. dutertrei 81 9040 ± 40 9560 ± 130 OS-33897 this study N. dutertrei 230 13,900 ± 35 15,820 ± 230 OS-33192 this study N. dutertrei 291 15,700 ± 85 18,440 ± 270 OS-33898 this study N. dutertrei 351 18,050 ± 65 20,630 ± 190 OS-33899 this study ME0005-27JC N. dutertrei 41 7430 ± 40 7730 ± 110 OS-33900 this study N. dutertrei 91 13,650 ± 65 15,470 ± 220 OS-33193 this study N. dutertrei 120 17,200 ± 70 19,750 ± 70 OS-33194 this study N. dutertrei 160 22,200 ± 95 26,180 ± 110b OS-33195 this study Y69-71P N. dutertrei 11–18 3240 ± 25 2870 ± 120 OS-45680 G. Mollenhauer and T. Eglinton, unpublished data, 2006 N. dutertrei 25–30 6110 ± 30 6370 ± 120 OS-45682 G. Mollenhauer and T. Eglinton, unpublished data, 2006 N. dutertrei 50 9760 ± 40 10,210 ± 150 OS-33894 Clark et al. [2004] Bulk CaCO3 85 12,130 ± 180 13,360 ± 200 (45) Clark et al. [2004] N. dutertrei 120 14,700 ± 65 16,830 ± 270 OS-33191 Clark et al. [2004] Bulk CaCO3 165 17,170 ± 350 19,670 ± 510 (45) Clark et al. [2004] N. dutertrei 180 19,150 ± 70 21,950 ± 370 OS-33895 Clark et al. [2004] N. dutertrei 260 28,000 ± 190 32,350 ± 170b OS-33896 this study aCalibrated to calendar ages with the software CALIB 5.0.2. [Stuiver and Reimer, 1993] using a reservoir correction of deltaR = 167 ± 106 yrs and the calibration data set of Hughen et al. [2004]. Calendar ages are rounded to the nearest 10 years. bReservoir corrected (467 years) and calibrated to calendar ages using Fairbanks et al. [2005]. PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 4 of 19 PA2213 3.3. Mass Accumulation Rates [20] Bulk accumulation rates (MARbulk) are derived from the product of linear sedimentation rates (cm/ka) and dry bulk densities (g/cm3) averaged over chosen core sections (see 3.5). The dry bulk density of cores ME0005-24JC, -27JC, TR163-19P and 31P was estimated from the carbonate content using the relationship r = 1/(3.6– 0.0279  %CaCO3) published by Snoeckx and Rea [1994]. Dry bulk density data for core Y69-71 are taken from Lyle et al. [2002], and data for core P7 are taken from Yang et al. [1995]. Mass accumulation rates of Corg and carbonate are derived as MARX =MAR (X)/100, where X is weight% Corg or CaCO3 averaged over the corresponding core sections. 3.4. The 230Th-Normalized Fluxes and Focusing Factors (y) [21] 230Th normalization relies on the approximation that the flux of scavenged 230Th reaching the seafloor is equal to its known production rate by 234U decay in the overlying water [Bacon, 1984; Suman and Bacon, 1989; François et al., 1990, 2004]. Sediment trap [Yu et al., 2001; Scholten et al., 2005] and modeling [Henderson et al., 1999; Marchal et al., 2000] studies indicate that deviations from this assumption do not exceed 30% over most oceanic regions. Consequently, there is a simple inverse relationship between the vertical flux of particulate material (Fv) and its scavenged 230Th activity which can be used to calculate preserved vertical fluxes from the activity of scavenged 230Th in the bottom sediment. Scavenged, or initial excess 230Th (xs230Th(0)), was derived by correcting the total 230Th activity for (1) contributions from detrital and authigenic sources using the activities of 232Th and 238U in the same samples and following principles summarized by François et al. [2004]; and (2) radioactive decay since the time of deposition using the chronologies described above. Estimates of total vertical flux (prFV–bulk) are derived from prFV–bulk = b  z/ex230Th(0), where b is the production of 230Th from 234U decay in the water column (0.0267 dpm m3 y1) and z is the water depth (m). Preserved vertical fluxes of sedimentary constituents such as Corg ( prFV–Corg), carbonate ( prFV–CaCO3), and opal (prFV–opal) are derived from prFVi = prFV–bulk  i/100, where i is weight percent Corg, carbonate, or opal. [22] In settings were particles settle through the water column and accumulate on the seafloor without lateral redistribution, the inventory of scavenged 230Th in the sediment should match the 230Th production in the over- lying water column integrated over the time of sediment accumulation. 230Th inventories in excess of production, on the other hand, are evidence of sediment focusing, while 230Th inventories lower than predicted from produc- tion are indicative of sediment loss, or winnowing, from the core site. Focusing factors (y :) are thus calculated as the decay corrected sedimentary accumulation rate of scavenged 230Th divided by its rate of production in the overlying water column integrated over the time interval represented by the core depth interval [Suman and Bacon, 1989]. Y ¼ Zr2 r1 230Thxs;0   rrdr bz t1  t2ð Þ where r1 is sediment depth (cm), t1 is the corresponding age (ka), and rr is mean dry bulk density (g/cm 3). The xs230Th0 Figure 3. (a) Downcore 230Th-normalized fluxes and (b) mass accumulation rates (MARs) of bulk sediment over the last 30 ka for all cores used in this study. MARs are averaged over the time intervals from the core top to 9.5, 9.5–13.4, 13.4–21, and 21–27 ka. Note different Y axes. PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 5 of 19 PA2213 and rr are averaged over the depth interval z1 to z2. Note that we recalculated y values for core Y69-71 here on the basis of 230Th values from Loubere et al. [2004], multiplied by 0.85 (see section 3.1) and using the new chronology described previously (see section 3.2). 3.5. Time Intervals Used for MAR and Focusing Calculations [23] We calculated MARs and focusing factors for OIS 1 (core top to 13 ka BP) and for OIS 2 (13–27 ka B.P). Note that for all cores, 0 cm core depth does not equal zero years. Although the definition of shorter time intervals may not necessarily be justified, particularly in cores TR163-31, TR163-19 and ME0005-27, which have a lower number of age control points, we nevertheless obtained MARs and focusing factors for the core top to 9.5, 9.5 to 13.4, 13.4 to 21, and 21 to 27 ka BP time intervals in order to facilitate comparison with the results of Loubere et al. [2004]. 4. Results 4.1. The 230Th-Normalized Fluxes [24] Th-normalized fluxes of bulk sediment in the Panama Basin region range from lower values during the Holocene to higher values during OIS 2 (Figure 3a). As expected for nearby sites, cores ME0005-24JC and Y69-71 show very similar Th-normalized bulk fluxes. Th-normalized fluxes of organic carbon range from low values during the Holocene to maximal values during the early deglaciation (Figure 4a). Note that the gradient between cores sites displayed by bulk and organic carbon fluxes is maintained throughout the last 30 ka. However, Th-normalized organic carbon fluxes differ by approximately 30% between nearby sites Y69-71 and ME0005-24JC (Figure 4a; see discussion in section 5.7). 4.2. Mass Accumulation Rates (MARs) and Sediment Focusing (y) [25] Traditional MARs are consistently higher than Th- normalized fluxes (Figures 3b and 4b). MARs of bulk sediment and Corg range from lower values during the Holocene to higher values during OIS 2. Both Corg and bulk sediment MARs display large and temporally variable gradients between core sites. During the 9.5–13.4 ka time interval, for example, bulk-MARs at site ME0005-24JC are almost 3 times higher than at neighboring site Y69-71. [26] As expected, focusing factors reflect the same tem- poral and regional trends displayed by bulk MARs (Figure 5) when calculated over the same time intervals. Similar to bulk MAR, the focusing factor is maximal (y = 7.9) at site ME0005-24 during the 9.5–13.4 ka time interval, implying that nearly 90% of the total sediment cannot be accounted for by vertical particle rain. This brief event is not evident in the other records. Holocene focusing factors are >2 at the foot of the Carnegie Ridge (sites ME0005-24JC and Y69-71) and Cocos Ridge (TR163-19P) indicating that more than 50% of the bulk sediment at these sites has been advected laterally during this period (Figures 5a and 5b). At all sites except ME0005-27 focusing factors are higher during OIS 2 (but see section 4.3). During OIS 2, y is 5.4 at ME0005-24JC, the highest measured for this period (Figure 5a). 4.3. Effect of Chronology on Focusing Factors [27] By definition, focusing factors and MARs are highly dependent on the age control of the sedimentary sequence. Figure 6a compares focusing factors and MARs for core Y69-71 calculated on the basis of the new stratigraphy used here and on the basis of the stratigraphy used previously [Loubere et al., 2004]. The shorter (in core depth) glacial interval based on the new stratigraphy significantly Figure 4. (a) Downcore 230Th-normalized fluxes and (b) MARs of organic carbon over the last 30 ka. MARs are averaged over the time intervals from the core top to 9.5, 9.5–13.4, 13.4–21, and 21–27 ka. Note different Y axes. PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 6 of 19 PA2213 decreases the MAR and focusing factor obtained for the interval from 21–27 ka BP. Acknowledging that the stage 2/3 boundary is difficult to define in d18O stratigraphies, we examine the effect of a ±1.5 ka age uncertainty at the OIS 2/3 transition (see error bars in Figure 6a). The lower focusing factors (4.4–2.6) and MARs obtained in this way for the 21–27 ka interval are not very different from those during the Holocene (y = 2.2). Similarly, if we were to reject the tuned age model altogether and rely on the radiocarbon date (at 32 calendar ka BP) to infer the core depth corresponding to the stage 2/3 boundary at 27 ka, focusing in the 21–27 ka time interval would decrease to 3.3, still higher than during the Holocene but significantly lower than previously estimated [y = 8.2, Loubere et al., 2004]. [28] On the basis of tight radiocarbon age constraints, Skinner and Shackleton [2005] recently suggested that the postglacial benthic d18O rise in the EEP lagged the benthic d18O rise in the deep NE Atlantic by 4 ka and the global Figure 6a. Comparison of bulk MARs (left) and focusing factors (right) of core Y69-71 calculated on the basis of the age model used here (solid line) and the previous age model (gray dashed line). Vertical lines indicate the error bars resulting from a ±1.5 ka uncertainty at the stage 2/3 boundary. Figure 5. Focusing factors for (a) the time interval of OIS 1 (core top–13 ka BP) andOIS 2 (13–27 ka BP) and (b) the time intervals from the core top to 9.5, 9.5–13.4, 13.4 to 21, and 21–27 ka. PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 7 of 19 PA2213 glacioeustatic d18O component by 2 ka because of local hydrographic effects in the deep Pacific. If we adjust the chronology of TR163-31P for this effect by subtracting 2 ka from core depths corresponding to the benthic d18O rise, less sediment is assigned to the glacial interval, making glacial MARs lower, which in turn translates into smaller glacial focusing factors (Figure 6b). Allowing an age uncertainty of ±1.5 ka at the OIS 2/3 transition could further Figure 6b. Comparison of bulk MARs (left) and focusing factors (right) of core TR163-31P calculated using the stratigraphy of Martin et al. [2002] (gray dashed lines), which is largely based on d18O correlation to SPECMAP and based on adjusting this chronology by 2 ka during the deglaciation to account for the potential lag of deep Pacific d18O versus the global glacioeustatic component suggested by Skinner and Shackleton [2005] (solid lines). Vertical lines indicate the error bars resulting from a ±1.5 ka uncertainty at the stage 2/3 boundary. Figure 6c. Comparison of bulk MARs (left) and focusing factors (right) of core ME0004-24JC calculated on the basis of the stratigraphy used here (solid lines) and on the basis of a radiocarbon age model which requires extrapolation from the oldest radiocarbon date at 20.6 ka to the OIS 2/3 boundary (dashed lines). Vertical lines indicate the error bars resulting from a ±1.5 ka uncertainty at the stage 2/3 boundary. PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 8 of 19 PA2213 reduce focusing factors and MARs (error bars in Figure 6b). Nevertheless, in the case of TR163-31P, the focusing factor and MAR during OIS 2 remain higher (y = 3–3.6) than during OIS 1 (y = 2) (Figure 6b). [29] The age model of ME0005-24JC used in this study is based on correlation of its down core carbonate profile to that of Y69-71 (see section 3.2). Taking the same ±1.5 ka age uncertainty at the OIS 2/3 into account illustrates that focusing factors and MARs during OIS 2 might not be significantly different from those observed during the 0–9.5 kyr time interval (Figure 6c). If, on the other hand, we were to reject the tuned age model and rely exclusively on the radiocarbon dates, we would have to linearly extrapolate sedimentation rates from the 14C age at 20 ka to the base of OIS 2 at 27 ka. Doing so increases the sediment interval corresponding to the 21–27 ka BP time interval, which in turn increases the corresponding MARs and focusing factors (y = 7.9–12.6) significantly over those observed in the 0–9.5 ka interval (y = 4.3, Figure 6c). Note also that the maxima in focusing and MAR between 9.5 and 13.4 ka BP in the carbonate based age model (Figures 3b and 5b) decrease in comparison with glacial time intervals when using the radiocarbon base age model (Figure 6c), once again illustrating the delicate dependence of focusing factors and MARs on core chronology. 4.4. Geochemistry [30] The down core record of ME0005-24JC exhibits a pronounced maximum in Fe/Al and Mg/Al ratios between 13.5 and 10 cal ka (Figures 7b and 7c), and Sinonbiogenic/Al and Mn/Al ratios are also elevated during this period (Table 3). This metal enrichment is also observed in the same time interval in nearby core Y69-71 (S. E. Calvert, unpublished data, 2006), but is absent in all the other cores considered here. The period of metal enrichment corresponds to the time of maximal y (Figures 5b and 7d) and MAR values (Figure 3b) in the carbonate based age model and a minimum in %CaCO3 content at site ME0005-24JC (Figure 7a). A more modest % CaCO3 minimum is also apparent at site Y69-71 at this time (Figure 7a). 5. Discussion 5.1. The 230Th-Normalized Fluxes and Focusing Factors in the Equatorial Pacific [31] The advantages of Th normalization are its relative insensitivity to stratigraphic errors and the possibility of a high-resolution, point-by-point determination of paleofluxes [François et al., 2004]. Earlier studies have also docu- mented a much higher degree of consistency in the sedi- mentary record of adjacent cores when using 230Th normalization versus MARs [e.g., Anderson et al., 2006; Loubere et al., 2004; François et al., 2004; Thomson et al., 1999; Frank et al., 2000, 1999; Rühlemann et al., 1996]. The same is clearly true for this study, where Th-normalized fluxes display a much more coherent pattern between core sites than MARs. (Figures 3 and 4). Both Th-normalized fluxes and MARs follow the trend expected from modern surface productivity (Figure 8), although absolute MARs are much higher than Th-normalized fluxes and there is a large difference between MARs at closely adjacent sites Y69-71 and ME0005-24JC. The difference in MAR values between these two sites is even larger prior to the Holocene (Figures 3b). This observation suggests that MARs, at least at site ME0005-24JC, are not solely driven by vertical flux. [32] Using chirp subbottom and seismic reflection profiles over sites ME0005-24JC and Y69-71, Lyle et al. [2005] noted a consistent bias of sediment deposition to the deeper basin over the entire depositional period (2.5 Ma yrs), with site Y69-71 collecting sediment at a rate 30% slower than the deeper site ME0005-24JC. On the basis of the depth of a major seismic horizon which has a mean depth of 15.7 m in the subbottom profile, but is found at 16.7 m at site Y69-71 and 24.3 m depth at sites ME0005-24JC, Lyle et al. [2005] estimated focusing factors of 1.1 (Y69-71) and 1.5 (ME0005-24JC), assuming that sediment focusing is supplied by local sediment redistribution within the area acoustically surveyed. The relative difference between these estimates (1.1/1.5 = 0.7) is consistent with the difference in 230Th-based focusing factors at both sites averaged over the last 27 ka (3.1 for Y69-71 versus 5.3 for ME0005-24JC; 3.1/5.3 = 0.6). Thus on this regional scale at least, there is good agreement between seismic and geochemical evidence for sediment focusing. Both methods thus show that, despite similar vertical fluxes at both sites (due to their proximity), there is more lateral input of sediment at the deeper site. The chief difference between the seismic and geochemical approach is that 230Th based estimates of focusing are much higher and suggest that both sites received an additional lateral input of sediment from outside the region acousti- cally surveyed. 5.2. Sources of Lateral Advection to Sites ME005-24JC and Y69-71 [33] We see two potential sources of laterally advected sediment to sites ME0005-24JC and Y69-71. The first one is general downslope transport of sediment from the sur- rounding Carnegie and Cocos Ridges into the southern boundary region of the Panama Basin. The second one is the episodic advection of hydrothermally influenced mate- rial, presumably from the Galapagos Spreading Center (see Figure 1 for location). 5.2.1. Downslope Transport [34] On the basis of seismic reflection profiles from the early 1970s, it has been known for some time that the sediment cover to the acoustic basement on the Carnegie and Cocos Ridges is thin and even partially absent [Van Andel et al., 1971]. Seismic imaging during ODP Leg 202 confirmed these observations for the eastern Carnegie Ridge [Mix et al., 2003]. Textural and compositional analyses revealed that the Carnegie and Cocos Ridges are indeed characterized by lag deposits mainly composed of coarse carbonate (intact planktonic foraminiferal shells), sand- sized ash particles and hydraulically equivalent volcanic minerals, whereas fine carbonate and opal are transported into the Panama Basin by downslope transport [Van Andel, 1973; Moore et al., 1973; Kowsmann, 1973]. Substantial sediment transport was also deduced from observations of transverse dunes and barchans in an erosional valley excavated into the northern flank of the Carnegie Ridge PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 9 of 19 PA2213 [Lonsdale and Malfait, 1974]. The valley itself is a several hundred meter deep depression cut into pelagic sediments. The dunes in the valley point northwestward, indicating down-valley sediment transport from the saddle in the central Carnegie Ridge into the Panama Basin. They are composed of sand-sized, broken (70%) and intact tests of Quaternary foraminifera [Lonsdale and Malfait, 1974]. [35] Although deep sea tidal currents are neither unidi- rectional nor continuous, they are often strong enough to entrain pelagic sediments and remove fine particles from the seafloor (>10 cm/sec, Beaulieu [2002],) especially in areas of high relief and where flow is channeled [e.g., Lonsdale et al., 1972; Cacchione et al., 2002; Shanmugam, 2003]. Such resuspension would automatically lead to downslope trans- port and preferential sediment accumulation in troughs such as the abyssal valley where sites Y69-71 and ME0005-24JC are located. Indeed, tidal currents reaching 15–20 cm/sec were observed in an erosional valley on the southern side of the Carnegie Ridge (Spiess et al. [1973], as cited by Lonsdale and Malfait [1974]), and barchans and related Figure 7. (a) Carbonate weight percent in core ME0005-24JC (solid gray line) and core Y69-71 (dashed gray line; data from Lyle et al. [2002]) and Th-normalized carbonate flux in core ME0005-24JC (solid black line) compared with (b) Fe, (c) Mg, and (d) focusing factors. Black lines indicate 230Th- normalized fluxes of Fe and Mg and gray lines indicate metal/Al ratios. PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 10 of 19 PA2213 dune forms generally indicate velocities of 40–100 cm/sec in restricted passages [Masson et al., 2004, and references therein]. 5.2.2. Hydrothermal Input [36] An additional source of laterally advected sediment could be the hydrothermal mound deposits located in an area of high heat flow south of the Galapagos Spreading Centre [Lonsdale, 1977; Corliss et al., 1978], which is approximately 50 nautical miles to the north of sites ME0005-24JC and Y69-71 (Figure 1). The bulk chemical composition of ME0005-24JC and Y69-71 is significantly different between 13.5 to 10 ka BP. During this time period, Fe/Al, Mg/Al, Mn/Al, and Si/Al ratios are elevated over values commonly observed in upper crust and basalt (Figures 7b, 7c, and Table 3). The hydrothermal deposits found south of the Galapagos Spreading Center are enriched in Fe-rich smectite (nontronite), which is characterized by extreme Al depletion (0.01–1.12 weight%) signifying the presence of Fe in the octahedral as well as the tetrahedral sites of this mineral phase. The hydrothermal deposits are also highly enriched in Mn and Si, and somewhat enriched in Mg compared to upper crust or basalt. They are thought Table 3. Summary of Major and Minor Element Data of Hydrothermal Deposits From the Vicinity of the Galapagos Rift in the Panama Basin Compared With Average Continental Crust and Basalt Upper Continental Crusta Average Basaltb Hydrothermal Depositsc ME0005-24JC During Eventd ME0005-24JC Before/After Evente Fe/Al 0.44 1.3 43 ± 8.7 4.2 0.75 Mg/Al 0.17 0.54 2.9 ± 0.6 2.9 0.5 Si/Al 3.8 2.8 44.7 ± 4.3 5.9f 2.5f Mn/Al 0.0074 0.0211 0.99 ± 0.64 0.63 0.15 aTaylor and McClennan [1985]. bFaure [1991]. cRatio of average metal to average Al concentration in well-crystallized nontronites dredged from hydrothermal sediment mounds south of the Galapagos Spreading Center (samples N1–N5 [Corliss et al., 1978]). dMaximal values during the %CaCO3 minimum event. eAverage values before and after the %CaCO3 minimum event. fOpaline Si was subtracted from total Si. Figure 8. Th-normalized fluxes and MARs of organic carbon (averaged from the age of the core top to 9.5 ka BP) versus modern primary production at the core sites [Antoine et al., 1996]. Both proxies display the regional gradient expected on the basis of modern conditions. However, MARs are larger and show a significant difference between sites ME0005-24JC and Y69-71. Site P7 is omitted because it only has one data point for the last 9.5 ka. PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 11 of 19 PA2213 to form by deposition of Fe, Mn and Si from hydrothermal fluids, which circulate through the basaltic crust and over- lying sediments in this region [Corliss et al., 1978]. The geochemistry of core ME0005-24JC thus points to the influence of allochthonous hydrothermal (nontronitic) material between 13.5–10 ka BP, which has diluted the carbonate fraction, thereby producing the marked %CaCO3 minimum in this core (Figure 7a). The addition of laterally sourced sediment during this brief time interval is consistent with the high focusing (Figure 7d) and MAR (Figure 3b) values based on the correlated age model at that time. It is also consistent with the slight decrease in Th-normalized CaCO3 fluxes during this time period (Figure 7a), as Th normalization is thought to somewhat underestimate the vertical particle flux of individual sediment components in settings where a deep nepheloid layer advects material with a composition that is different from that found at the final deposition site [François et al., 2004]. Nearby core Y69-71 also displays a drop in %CaCO3 at this time (Figure 7a), as well as enrichments in Fe, Si and Mg (not shown) indicating that this site was also affected by hydrothermal input, albeit to a lesser extent. [37] These two sources of sediment, the Carnegie Ridge and the Galapagos Spreading Center lie outside the sub- bottom profile presented by Lyle et al. [2005], suggesting that their acoustically surveyed section might not represent a Figure 9. Focusing factors (Y) in the equatorial Pacific during (a) the Holocene, (b) the last glacial period, and (c) the ratio of glacial to Holocene focusing factors in the eastern equatorial Pacific. Data and references are reported in Table 4. PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 12 of 19 PA2213 closed system with respect to sedimentation. This implies that their claim that 230Th normalization overestimates sediment focusing is unwarranted. 5.3. Local Differences in the Degree of Focusing in the Panama Basin and Regional Sediment Mass Balance [38] The compilation of data from the Panama Basin in Figure 5 indicates that focusing factors are highly variable in time and space. High values are restricted locally to the area of the seafloor at the foot of the Carnegie Ridge (ME0004-24JC and Y69-71) and the Cocos Ridge (TR163-19P). They are less pronounced on the slope of the Carnegie Ridge (ME0005-27JC) and do not extend far into the Panama Basin (P7). This is consistent with the view that sediment focusing and winnowing are controlled by bathymetry and current flow on a local scale [e.g., Turnewitsch et al., 2004; Loubere et al., 2004; Scholten et al., 1994]. [39] On the basis of earlier findings of very high glacial focusing factors at site Y69-71 (y = 8.2; Loubere et al. [2004], Lyle et al. [2005] disputed the validity of 230Th- normalized fluxes by arguing that such high sediment focusing extrapolated over the entire region where they have identified a glacial MAR maximum (a  6 square area) would necessitate a source region barren of sediment covering a 17 square area, which would be easily noticed but has not been observed in the equatorial Pacific [Lyle et al., 2005]. Our data show, however, in light of the spatial and temporal heterogeneity of focusing factors reported here, that extrapolating a focusing factor estimated from one site to the entire EEP cannot be justified. In addition, the original glacial focusing factors reported at site Y69-71 need to be revised down significantly (see section 4.3 and below), further decreasing the need for an inordinately large source region to account for the glacial increase in focusing. 5.4. Focusing Factors in the Central and Eastern Equatorial Pacific [40] Focusing factors reported thus far for the central and eastern equatorial Pacific region are summarized in Figure 9 Table 4. Focusing Factors (Y) in the Central and Eastern Equatorial Pacific Core id Latitude Longitude Depth, m Y Holocene Y Glacial Y Gl/Y Hol Reference TT013 MC112 5.00N 140.00W 4560 1.0 Berelson et al. [1997] TT013 MC34 5.00S 140.00W 4391 1.1 Berelson et al. [1997] TT013 MC27 3.00S 140.00W 1.1 Berelson et al. [1997] TT013 MC97 2.00N 140.00W 4540 1.1 Berelson et al. [1997] TT013 MC69 0.00N 140.00W 4440 1.9 Berelson et al. [1997] TT013 MC19 2.00S 140.00W 4475 1.9 Berelson et al. [1997] 61 BX1 0.91N 140.04W 4328 1.4 1.9 1.4 Yang et al. [1990] MANOP B25 1.05N 139.02W 4401 0.7 0.8 1.1 Marcantonio et al. [2001] TT013-PC18 2.00S 139.00W 4354 2.8 0.7 0.3 Marcantonio et al. [1996] TT013-PC72 0.00N 139.00W 4298 2.3 2.3 1.0 Marcantonio et al. [1995] MANOP B18 1.06N 138.80W 4281 0.9 0.6 0.7 Marcantonio et al. [2001] 54 BX1 1.01N 133.70W 4212 1.5 2.0 1.3 Yang et al. [1990] 53 BX1 0.98N 124.63W 4516 1.8 3.0 1.7 Yang et al. [1990] 52 BX1 1.01N 118.20W 3857 1.2 1.8 1.5 Yang et al. [1990] ODP-849B 0.18N 110.52W 3851 2.1 3.0 1.4 Pichat et al. [2004] 50 BX1 1.03N 104.41W 3473 1.8 2.3 1.3 Yang et al. [1990] RC13-110 0.10N 95.65W 3231 2.0 1.6 0.8 Loubere et al. [2004] ODP-846B 3.10S 90.82W 3307 2.1 3.7 1.8 Loubere et al. [2004] ME0005-24JC 0.02N 86.46W 2941 4.9 5.5 1.1 this study Y69-71 0.10N 86.48W 2740 2.5 3.6 1.4 this study P7 2.60N 83.79W 3085 1.2 1.9 1.6 this study Y71-6-12 16.45S 77.57W 2734 1.4 0.9 0.6 S. S. Kienast et al., unpublished data, 2006 ME0005-27JC 1.85S 82.79W 2203 1.8 1.7 0.9 this study VNT01-8PC 0.03N 110.48W 3791 1.6 2.3 1.4 S. S. Kienast et al., unpublished data, 2006 TR163-19 2.26N 90.95W 2348 2.2 2.5 1.1 this study TR163-31 3.60S 83.95W 3209 1.6 3.4 2.1 this study V21-40 5.52S 106.76W 3128 3.5 3.2 0.9 S. S. Kienast et al., unpublished data, 2006 V19-28 2.37S 84.65W 2720 2.0 3.5 1.8 Lao et al. [1992] V19-29 3.58S 83.93W 3157 2.4 2.4 1.0 Lao et al. [1992] KLH 093 1.50N 102.06W 3260 2.1 2.5 1.2 Frank et al. [1994] KLH 068 1.23N 101.61W 2870 1.3 1.6 1.2 Frank et al. [1994] RC13-140 2.87N 87.75W 2246 2.9 3.6 1.2 L. I. Bradtmiller et al., unpublished data, 2006 RC11-238 1.52S 85.82W 2573 3.0 2.0 0.7 L. I. Bradtmiller et al., unpublished data, 2006 V19-30 3.38S 83.52W 3091 3.2 4.4 1.3 L. I. Bradtmiller et al., unpublished data, 2006 RC13-114 1.65S 103.63W 3436 3.8 2.2 0.6 L. I. Bradtmiller et al., unpublished data, 2006 PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 13 of 19 PA2213 and Table 4. At most sites, focusing factors are greater than one during the Holocene (Figure 9a). This is not surprising given that high-sedimentation sites are preferentially chosen for coring operations because of their expected high tem- poral resolution. The compilation also reveals that focusing factors are generally higher in the eastern equatorial Pacific, particularly in the vicinity of the Panama Basin. This observation is consistent with the view that topographic relief should favor downslope sediment transport and focusing. Note, however, that a more modest, but still prevalent focusing effect is also found at sites between 95 and 140W and 0 and 2N, far away from major topographic features. Another remarkable observation is the relative increase in focusing during the last glacial period apparent at many sites, especially those near topographic features (Figure 9c). 5.5. Possible Mechanisms for Higher Glacial Focusing Factors [41] We see two principal ways to explain the higher glacial focusing factors observed in the EEP. One possibility is that the glacial increase in focusing in this EEP is only apparent and partly or largely results from inaccurate age control. Focusing factors are essentially the accumulation rate of scavenged 230Th divided by its rate of production, and thus the largest source of uncertainty in estimates of focusing comes from uncertainties in age models and MARs. Very high focusing factors (y = 8.2) were reported for the 23–27 ka time interval of core Y69-71 on the basis of an earlier chronology [Loubere et al., 2004]. Using the revised chronology now available for this core (see section 3.2), MARs and focusing factors are reduced here by more than a factor of 2 (y = 3.6) for this time interval. Allowing for a ±1.5 ka age uncertainty at the stage 2/3 boundary could either increase or further reduce focusing and MARs in this time interval (y = 4.4–2.6), with the reduced values being much closer to Holocene ones (y = 2.2; Figure 6a). In core ME0005-24JC, which displays the highest overall focusing values and MARs observed in this study, a ±1.5 ka age uncertainty could similarly increase or reduce the difference between Holocene and glacial focusing and MARs (Figure 6c). In core TR163-31, the same error would still leave glacial focusing factors slightly higher than Holocene ones (Figure 6b). It is obvious that focusing factors and MARs are highly sensitive to the age model, and it is possible that the apparent increase during the glacial period observed here might be partly due to inaccuracies in age control. Many of the records compiled in Figure 9 are dated using d18O stratigraphies, in which the base of glacial stage OIS 2 at 27 ka BP is notoriously difficult to identify. Additional uncertainty has recently been implied during the deglaciation and at the beginning of OIS 2. Skinner and Shackleton [2005] suggested that the postglacial benthic d18O rise in the EEP lagged the benthic d18O rise in the deep NE Atlantic by 4 ka and the global glacioeustatic d18O component by2 ka because of local hydrographic effects in the deep Pacific. If true, this effect would have led to an overestimation of the thickness of the glacial sediment intervals in previous studies based on d18O stratigraphies in the Pacific, rendering glacial focusing factors and MARs erroneously high. Previously published Holocene focusing factors and MARs might also not be free of uncertainties. Piston cores often overpenetrate the sediment during coring operations, which leads to a real age of the top most core sample that is unknown and non zero. Assigning an age of zero years to the core top, however, results in a longer time interval for the Holocene core interval. This results in MARs and focusing factors that are erroneously low, thereby further enhancing the apparent glacial-interglacial contrast in focusing factors and MARs. Analyzing multi- cores with undisturbed sediment surfaces together with piston/gravity cores, such as done in the Southern Ocean [Frank et al., 2000], would allow evaluation of this potential bias. [42] If, on the other hand, we assume that the increase in glacial focusing is real and not solely driven by uncertain- ties in age control, we need a mechanism that can explain this general increase in sediment redistribution during glacial periods. One possibility could be related to an increase in tidal dissipation during glacial stages. Wunsch [2003] suggested that tidally induced ocean mixing should have increased during the LGM because of an increase in deep ocean tidal dissipation when shallow energy sinks were removed by lower sea level stands. Recent modeling studies indeed suggest that globally averaged barotropic tidal kinetic energies and deep ocean dissipation were significantly greater for LGM bathymetries [Egbert et al., 2004; Arbic et al., 2004]. Since there is significant dissipa- tion of tidal energy over rough topography in the open ocean [Egbert and Ray, 2000, 2001], this effect could have been particularly strong in the Panama Basin area in view of the rugged local seafloor topography. The overall increase in tidal dissipation would have caused an enhancement in abyssal tidal currents and is likely to have resulted in greater entrainment and redistribution of sediment particles. The tidally induced forcing of sediment redistribution proposed here is time variant and thereby addresses one of the requirements of Paytan et al. [2004] for a climatically driven physical mechanism to explain glacial-interglacial changes in sediment focusing. 5.6. Paleoproductivity Reconstructions in the EEP From Th-Normalized Fluxes of Organic Carbon [43] Despite the difference between MARs and 230Th-normalized fluxes in the Panama Basin, both proxies show overall higher Corg fluxes in OIS 2. These findings are in qualitative agreement with previous studies pointing to higher export production during OIS 2 [Pedersen, 1983, 1988; Farrell et al., 1995; Yang et al., 1995; Herguera, 2000; Lyle et al., 2002]. However, 230Th normalized Corg fluxes are maximal during the deglaciation (18–13 ka BP) rather than the full glacial per se, suggesting enhanced export production or organic matter preservation at that time, which is consistent with a recent study identifying the time interval from 20–15 ka BP as the period of most intense upwelling in the EEP over the last 40 ka [Martinez et al., 2006]. [44] On the other hand, higher glacial 230Th-normalized Corg fluxes are at odds with lower estimates of paleoexport production during OIS 2 in the Panama Basin based on a PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 14 of 19 PA2213 benthic foraminiferal transfer function [Loubere et al., 2003]. Both methods have been applied at site Y69-71, and lead to opposite results (Figure 10). This discrepancy is perplexing, and unresolved at the time of writing. Benthic foraminiferal assemblages are known to record the relative changes in the flux of labile organic carbon to the seabed [e.g., Kuhnt et al., 1999; Loubere and Fariduddin, 1999; Wollenburg and Kuhnt, 2000], as does the 230Th normalized organic matter burial. Further work will be needed to resolve this discrepancy. 5.7. Difference in 230Th-Normalized Organic Carbon and Opal Fluxes Between Sites Y69-71 and ME0005-24JC [45] 230Th-normalized organic carbon fluxes are approx- imately 30% higher at deeper site ME0005-24JC compared to Y69-71 from 27 to 9 ka BP (Figures 4a and 11a). A similar offset between both sites is observed in 230Th- normalized opal fluxes (Figure 11b). Sedimentation rates (Figure 2) and focusing factors (Figure 5b) are also signif- icantly higher at ME0005-24JC than at site Y69-71 in the time interval from 27 to 9 ka BP. Thorium normalized fluxes of bulk sediment on the other hand which are dominated by carbonate are very similar at both sites throughout the last 30 ka (Figure 3a). The higher 230Th normalized biogenic fluxes at site ME0005-24JC compared to Y69-71 are related to higher weight percentages of these constituents at the former site, which translate directly into higher 230Th-normalized flux estimates (see equations in section 3.4). At least for organic carbon, analytical differ- ences between ME0004-24JC and Y69-71 (see section 3.1) cannot fully account for the intersite difference, as an offset remains even when using organic carbon data produced by the same laboratory (Figure 11a). We recognize three non exclusive possibilities to explain the difference in weight percentages and hence 230Th normalized fluxes of organic carbon and opal at these sites: [46] 1. Higher sedimentation rates at ME0005-24JC could have led to faster burial and better preservation of organic carbon and biogenic opal at this site compared to Y69-71 [sensu Müller and Suess, 1979]. [47] 2. A subtle increase in carbonate dissolution with depth would lead to increased weight percentages of organic carbon, opal as well as terrigenous material at site ME0005- 24JC, which is 200 meters deeper than site Y69-71. Indeed, %opal and %terrigenous material (not shown) are slightly higher in core ME0005-24JC than in core Y69-71, where as %carbonate is slightly higher in core Y69-71 (Figure 7a). [48] 3. Preferential removal and advection of organic matter and opal concentrated in the fine sediment fraction to site ME0005-24JC offers a third explanation. In this scenario, the preferential advection of a minor sediment constituent such as organic carbon or opal would not significantly affect the 230Th-normalized flux of bulk sed- iment and major sediment constituents, but would increase the %Corg and % opal at the receiving site, resulting in higher 230Th-normalized values of these constituents (see section 3.4). [49] These possibilities need to be investigated further, particularly in light of the discrepancy with paleoproduc- tivity reconstructions based on benthic foraminiferal trans- fer functions (Figure 10). It is possible that this discrepancy might be related, in part, to a possible preference of benthic foraminifera for very fresh organic matter delivered directly Figure 10. 230Th-normalized organic carbon flux compared to paleoproductivity estimates based on benthic foraminifera [Loubere et al., 2003] at site Y69-71. PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 15 of 19 PA2213 from the sea surface versus laterally advected organic matter which could be more refractory. However, we note that the pattern of 230Th-normalized Corg flux at ME0005-24JC strongly resembles that at other sites in the Panama Basin, including sites ME0005-27JC and P7, which are only marginally affected by focusing (Figures 4a, 5a, and 5b). Hence we suspect that while preferential advection of organic carbon (and opal) under conditions of elevated focusing is possible, it is not the dominant control on the Th-normalized organic carbon and opal fluxes in core ME0005-24JC. 6. Summary and Conclusions [50] The use of Th normalization as a tool for recon- structing past particle fluxes from the sea surface to the seafloor is still controversial [Lyle et al., 2005; François et al., 2007]. This study shows that 230Th-normalized fluxes of bulk sediment and organic carbon display a regionally coherent pattern in the EEP, which is consistent with present-day surface oceanographic conditions. Nearby sites show almost identical 230Th-normalized bulk fluxes and a 30% difference in 230Th-normalized Corg fluxes. Traditional MARs of bulk sediment and Corg, on the other hand, are significantly higher, and display large site-to-site variability. Thus the results of this study further validate 230Th normalization. [51] Holocene focusing factors are 2–4 at the foot of the Carnegie Ridge, suggesting that lateral sediment transport to this region is significant. This observation is consistent with earlier observations of lag deposits and bare rock on top of the Carnegie Ridge and of an erosional valley on the basin- facing slope of the ridge. The relative difference between focusing factors at two nearby sites the Panama Basin estimated by 230Th normalization and using seismic profiles [Lyle et al., 2005] is comparable. [52] Sites that are affected by focusing in the Holocene show even higher focusing factors during OIS 2, similar to previous findings in the central and eastern EEP. Examina- tion of the effect of chronological uncertainties at the OIS 2/3 and 1/2 boundaries in our records shows that the magnitude of the glacial increase in focusing factors and MARs is very sensitive to chronological uncertainties. We thus offer two possible explanations for the glacial increase in focusing and MARs. The first one is that the apparent increase in lateral sediment redistribution is partly or even largely an artifact of insufficient age control in the EEP. The second explanation, which assumes that the observed increase is real, invokes enhanced deep sea tidal current flow during periods of low sea level stand [Wunsch, 2003]. Only improved stratigraphic control will help to distinguish between these two scenarios. [53] The controversy revolving around 230Th normaliza- tion was partly triggered by very high estimates of glacial focusing (y = 8.2) at site Y69-71 in an earlier study [Loubere et al., 2004]. Extrapolating from this site to the entire EEP, Lyle et al. [2005] assumed the need for a sediment source covering a 17 square area to account for the high focusing in the Panama Basin during the LGM, which is not observed in seismic surveys. Using improved chronological control at site Y69-71, we show here that glacial focusing values have to be revised down consider- ably (y = 4.4–2.6), although lateral sediment input is still considerable. In addition, the large spatial and temporal heterogeneity of focusing factors observed in the EEP and elsewhere does not warrant extrapolation from one site to the entire region. Thus there appears to be no requirement Figure 11. Th-normalized fluxes of organic carbon (a) and biogenic opal (b) at sites ME0005-24JC and Y69-71. Note that the difference in organic carbon fluxes between both sites largely remains when using Corg data produced by the same laboratory (OSU) for the flux calculations. Percent organic carbon data of ME0005-24JC used for Th-normalized flux calculations are from this study (red solid line), from Lyle et al. [2005], red dashed line), and from Lyle et al. [2002] for core Y69-71 (blue line). Percent biogenic opal data used for Th-normalized flux calculations are from this study (ME0005-24, red line) and Lyle et al. [2002], Y69-71, blue line). PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 16 of 19 PA2213 for an inordinately large area of seafloor devoid of sediment to account for the mass of laterally supplied sediment during the glacial. [54] Over the course of the last 30 ka, both 230Th- normalized fluxes and MARs of Corg show a general increase in OIS 2 compared to the Holocene. Th-normalized Corg fluxes are maximal in the deglaciation, similar to Th- normalized opal fluxes. This could indicate enhanced export production at that time, in conflict with results inferred on the basis of a benthic foraminifera transport function in the Panama Basin [Loubere et al., 2003]. [55] Although 230Th-normalized bulk fluxes are nearly identical at two nearby sites, there is a 30% difference in 230Th-normalized fluxes of organic carbon and opal between these sites. This apparent difference in 230Th- normalized fluxes is caused by a difference in weight% of these constituents at the two sites. The difference in weight%, in turn, could be caused by either changes in sedimentation rate or carbonate dissolution with depth. Alternatively, preferential advection of minor sediment constituents associated with fine-grained particles such as opal and organic matter might have increased the concen- tration of these constituents and their 230Th-normalized fluxes at the deeper site. These observations may poten- tially hold clues to help explain the difference between results of paleoproductivity reconstructions based on ben- thic transfer functions and other proxies. [56] Acknowledgments. We gratefully acknowledge official reviews by Robert Anderson, Mitchell Lyle, Martin Frank, and one anonymous reviewer which helped to improve and clarify the manuscript. We also wish to acknowledge fruitful discussions with Zanna Chase, Gesine Mollenhauer and Tim Eglinton. Gesine Mollenhauer, Tim Eglinton, and Louisa Bradtmiller shared unpublished 14C data. Maureen Soon, Alan Fleer and Susan Brown-Leger provided invaluable technical assistance. 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Kienast, Department of Oceanography, Dalhousie University, 1355 Oxford Street, Halifax, Nova Scotia, B3H 4J1 Canada. (stephanie.kienast@dal.ca) A. C. Mix, College of Oceanic and Atmo- spheric Sciences, COAS Administration Build- ing 104, Oregon State University, Corvallis, OR 97331-5503, USA. PA2213 KIENAST ET AL.: PARTICLE FLUX IN THE PANAMA BASIN 19 of 19 PA2213

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