Case Study Dr. Tabitha Ndungu presented to NACADA on their 2nd Conference in Nairobi, Kenya Date; 10th - 14th JUNE 2013 Venue: Moi Sports Centre Kasarani Gymnasium Theme: " The Youth and Drugs: A Call to Action." In spite of the damage done by
mais n'ont pas d'effets néfastes pour l'organisme dans son ensemble.
NAKATSUKA ET AL.: DOC AND POC IN THE SEA OF OKHOTSK of young DOC (14C age) from the mixed water region offnorthern Japan. They also suggested that one source area forthe young DOC into the NPIW is the Sea of Okhotsk,according to the previous reports for the water ventilationprocess in this area [Yasuda et al., 1996; Talley, 1997].
 In relation to this background, we have reported material transport from the continental shelf to thedeep sea in the Sea of Okhotsk using a turbidity profiler[Nakatsuka et al., 2002]. The Sea of Okhotsk is a marginalsea located on the northwestern rim of the Pacific Oceanand is known as a seasonal sea ice area [Alfultis and Martin,1987; Kimura and Wakatsuchi, 2000]. A large volume ofcold brine water is rejected and settles on the bottom of thenorthwestern continental shelf along the Siberian coastduring sea-ice formation in winter [Martin et al., 1998;Gladyshev et al., 2000]. Even after entraining the sea-icebrine, the density of the bottom water on the shelf (denseshelf water, DSW) generally does not exceed 27.0 sq,reflecting the inflow of Amur River water. Therefore, coldbrine water does not spread to the deep layer but ratherpenetrates to the intermediate depths (200 – 500 m) to mixwith the Okhotsk Sea Intermediate Water (OSIW) [Kitani,1973; Wong et al., 1998; Itoh et al., 2003], which finallyflows out of the Sea of Okhotsk to join the formation ofNPIW [Talley, 1991]. Because the DSW always containslarge amounts of resuspended sedimentary particles due to a Map of the observed area in the Sea of Okhostk.
strong tidal mixing on the shelf [Kowalik and Polyakov, Open and solid circles are the sites of measurements of 1998], the outflow of DSW results in a large flux of dissolved and particulate organic carbon. Line-54N and particulate materials from the shelf to the open ocean Line NE correspond to the sections illustrated in Figures 2 [Nakatsuka et al., 2002]. In spite of the temporal sea-ice and 3, respectively. Solid circles indicate the sites where cover, the primary productivity of the Sea of Okhotsk is profiles in the water column are shown in Figures 4 and 6.
very high, especially on the continental shelf [Sorokin and Arrows in the smaller figure show the main direction of Sorokin, 1999; Saitoh et al., 1996], due to the relatively water current in the Sea of Okhotsk.
high insolation and the major nutrient and micronutrientinput from the Amur River. Therefore DSW flowing intoOSIW may export not only the resuspended sedimentaryparticles but also fresh organic matter produced on the shelf.
of Okhotsk (Figure 1). The stations for water sampling were  In order to evaluate the role of dense water outflow in located on the northwestern continental shelf, off the transporting biologically produced materials from the shelf northeastern coast of Sakhalin Island and the area near the to the deep open ocean, in addition to particulate matter, it is Amur River mouth. These stations were arranged so as to necessary to measure the dissolved organic matter. The clarify the effect of the Amur River discharge and DSW spatial distributions of DOC and POC in the Sea of Okhotsk outflow for the transport of organic matter through the have been investigated [Agatova et al., 1996]. However, the continental shelf areas to the OSIW in the Sea of Okhotsk, mechanisms determining their distributions have not yet which finally connects to the North Pacific Ocean.
been clarified. We present here the data sets of both POC  Sampling was carried out throughout the water and DOC in the Sea of Okhotsk, including the continental column at every sampling station using a Seabird CTD-Water shelf and slope areas as well as the area near the Amur River sampling system equipped with 24 10-L Niskin bottles.
mouth. Using these data, we discuss the effects of dense Approximately 30 mL of water was poured directly into a water outflow and river water input for the transport of 40-mL precleaned (and precombusted) glass vial from the organic matter through the continental shelf area in the Sea valve of each Niskin bottle, and the glass vials with water of Okhotsk, possibly to the North Pacific Ocean. The stable samples were tightly capped with clean rubber-sealed screw carbon isotope ratios (d13C) of particulate organic carbon caps and immediately stored in a freezer ( 30C) until total (POC) and the chlorophyll concentrations (Chl-a) were organic carbon analyses at a shore-based laboratory.
measured in order to assess the origin of POC.
 Another 1000 mL of water was collected in a plastic bottle, and immediately filtered onto a 450C precombustedWhatman GF/F filter of 25 mm diameter on board. The Materials and Analytical Methods filters with suspended particles were packed into aluminum Water Sampling and Sample Preparations foil and stored in a freezer ( 30C) until particulate organic  Water samples for organic carbon analyses were carbon analyses in the laboratory. However, water samples collected in June 2000 during a research cruise with R/V could not be filtered at layers shallower than 100 m at the Professor Khromov (Far Eastern Regional Hydrometeoro- three sites in Line-54N (Figure 1) off the northeastern logical Research Institute, Vladivostok, Russia) in the Sea Sakhalin Island due to the limited time aboard ship.
NAKATSUKA ET AL.: DOC AND POC IN THE SEA OF OKHOTSK  For the measurement of Chl-a, 200 mL of water was analyzed the stable carbon isotopic ratio of POC, using a collected in a dark plastic bottle at each layer shallower than continuous flow system (ThermoQuest, Conflo-II), which 200 m at every sampling site. The water samples were introduces the CO2 gases with He carrier discharged from immediately filtered onto the 25-mm diameter Whatman the elemental analyzer directly into the isotopic ratio GF/F filters. The filters were inserted into plastic tubes mass spectrometer (ThermoQuest, Delta-Plus). The stable together with 6 mL of dimethyl formamide solution and carbon isotopic ratio is represented as d13C, where d13C = then stored, wrapped in aluminum foil, in a freezer ( 30C) 1] 1000 (%), and the until the Chl-a analyses. Along an east-west transect on standard deviation of the measurement is within 0.2%.
54N off the northeastern Sakhalin Island, water samples forChl-a measurement were collected not only at 0- to 200-m Chlorophyll a (Chl-a) depths but also throughout the water column to its bottom in  The amounts of the extracted chlorophyll a and phaeo- order to detect the transport of fresh organic matter into the pigment in dimethyl formamide solutions were measured ocean interior by DSW outflows.
using a fluorescence spectrophotometer (Turner, 10-AU) inthe laboratory of Sei-ichi Saito, at the Graduate School of Total Organic Carbon (TOC) Fishery Science, Hokkaido University.
 Frozen water samples in 40-mL glass vials were Turbidity Profiles in the Water Column thawed in running water and homogenized for 10 min by ultrasonic vibration. A volume of 100 mL of 6N HCl During the CTD/water sampling, a laser forescattering type of turbidity meter (ALEC Denshi, ATU6-8M) was solution was added into the 10 mL of melted water, and attached to the frame of the water sampler. This instrument all carbonate materials were purged by bubbling with pure directly presents turbidity data in parts per million, according air for 10 min. The decarbonated waters were directly to a conversion factor determined using kaolinite suspensions analyzed for the TOC, including dissolved and suspended in the factory [Nakatsuka et al., 2002].
organic carbon, using a TOC analyzer (Shimadzu, TOC-5000). The concentration of dissolved organic carbon(DOC) was determined by the subtraction of particulate Results and Discussions organic carbon (POC) content, which was measured as  We illustrate two-dimensional sections of tempera- described below, from TOC content.
ture, salinity, density, turbidity, DOC, POC, Chl-a, and d13C  Each water sample was measured 3 times, with the of POC along Line-54N and Line-NE (Figure 1) in Figures 2 mean peak area taken to determine concentrations. The and 3, respectively, using Ocean Data View (R. Schlizer, TOC content for each water sample was calculated using a calibration line, which was created before the analyses of 2002), and explain the spatial distributions of those prop- sample waters every day, by the combustion of waters erties and discuss their causes in detail.
containing standard reagents (potassium hydrogen phtha-late). The ultra-pure water (Milli-Q water) used for dilution of the reagent always contained approximately 7 mM of  We can find two very cold water masses (< 1C) in organic carbon contamination, which must be attributed to this section (Figure 2a). Both are located at between 50 and either the ultra-pure water (water blank) or the TOC 100 m in depth; one is on the shelf and the other is above analyzer itself (instrument blank). In the present study, we the deep basin. Because the salinity is different between assumed that the 7 mM of organic carbon originated from those two cold regions (Figure 2b), the former has a the ultra-pure water itself, and we then calculated the potential density of 26.7 – 26.9 sq, which is equivalent to contents of TOC in the water samples using the slope of that of the intermediate water mass between 200 and 400 m calibration lines. If the 7 mM of organic carbon contains far below the latter mass (Figure 2c). The cold and dense instrument blank as well, the results of TOC in the present water mass on the shelf can be regarded as the DSW, which study must be overestimated to a certain degree. However, has been produced by the rejection of saline brine water this does not affect our primary discussion, because the from sea ice during the last winter [Martin et al., 1998; amount of the blank carbon is very small and is almost Gladyshev et al., 2000]. On the other hand, the offshore constant (7.3 ± 0.3 mM) compared with the actual range of cold subsurface water is called the ‘‘dichothermal layer,'' TOC concentration measured in the Sea of Okhotsk (60 – which was formed by the cooling of the pelagic surface 450 mM). The standard deviation was usually within 1 – water in winter and which can be found all over the open 2 mM (1s) for each sample measurement.
area in the Sea of Okhotsk. In relation to the higher densityof the DSW, it is important to note the existence of a low- Particulate Organic Carbon (POC) and Stable temperature intermediate water mass (<1C) on the slope Carbon Isotopic Ratio (D13C) of POC (300 – 450 m), which is obviously colder than surrounding  Frozen 25-mm GF/F filters, which contain POC, were waters (Figure 2a). Because the density range of this water thawed and first acidified by the addition of several drops of mass, 26.8 – 26.9 sq, is almost identical to the DSW on the 20% HCl to remove all carbonate materials. After drying the shelf, this intermediate cold water mass on the slope must GF/F filters by leaving them in a clean glass desiccator for 1 be affected by the discharged DSW from the continental to 2 days together with a dish of NaOH pellets and P2O5 shelf. Both the DSW and the cold slope water mass had a powder, the filters were cut and wrapped with large tin high turbidity (Figure 2d), suggesting the same origin of capsules and then measured with respect to carbon content these water masses [Nakatsuka et al., 2002].
using an elemental analyzer (Fisons, NA-1500). In order to  The cold intermediate water mass on the slope is also discuss the origin of POC in the Sea of Okhotsk, we also rich in organic matter. Concentrations of both DOC and
NAKATSUKA ET AL.: DOC AND POC IN THE SEA OF OKHOTSK Vertical sections of (a) temperature, (b) salinity, (c) potential density, (d) turbidity, (e) dissolved organic carbon (DOC), (f) particulate organic carbon (POC), (g) Chl-a, and (h) stable carbonisotopic ratio (d13C) of POC along Line-54N.
NAKATSUKA ET AL.: DOC AND POC IN THE SEA OF OKHOTSK Vertical sections of (a) temperature, (b) salinity, (c) potential density, (d) turbidity, (e) dissolved organic carbon (DOC), (f) particulate organic carbon (POC), (g) Chl-a, and (h) stable carbonisotopic ratio (d13C) of POC along Line-NE.
NAKATSUKA ET AL.: DOC AND POC IN THE SEA OF OKHOTSK near the surface, which induces the increase in temperaturein the uppermost layer (Figure 2a). This fresh surface waterhas a very large amount of DOC (Figure 2e), which musthave originated from the river water, while the POCconcentration of this water mass is not larger than thesubsurface layer on the slope area (Figure 2f). The Chl-aconcentration has its maximum value, more than 9 mg/L, atthe subsurface layer on the slope area, showing the presenceof the phytoplankton bloom at the time of water samplingthere (Figure 2g). POC also has its maximum value atthe same position of the phytoplankton bloom, while DOCshows a significant but very small increase at this position.
These correlations between DOC, POC, and Chl-a suggestthat POC is produced mainly by marine organisms; how-ever, most of the DOC in this area originates from riverwater.
 On Line-NE (Figure 3), the characteristics are principally the same for the distributions of physical andchemical properties as those in Line-54N describedabove. The cold water masses, which have the densityrange from 26.7 to 26.9 sq, are located on the shelf andthe slope (Figures 3a and 3c). Both water masses have high Vertical profiles of (a) temperature, (b) potential turbidity (Figure 3d) and high concentrations of DOC and density, (c) POC and Chl-a, and (d) d13C of POC at site 82.
POC (Figures 3e and 3f), and the d13C of POC is higher than 20% in the two water masses.
 In the surface layer, a low-salinity water mass exists POC are distinctly higher than in the surrounding water at the site closest to the coast (Figure 3b), which has very mass (Figures 2e and 2f). Chl-a concentration in the cold high DOC concentration (Figure 3e). As in Line-54, Chl-a intermediate water is also significantly higher than in the and POC have their maximum values at the subsurface layer pelagic water at the same depth level, suggesting a rapid above the slope region (Figures 3f and 3g). Interestingly, the outflow of DSW from the continental shelf together with d13C at the maximum center of POC is very low (< 24%) fresh biogenic particles (Figure 2g). The distribution in d13C (Figure 3h), indicating the effect of low growth rate for the of POC shows a tight linkage of the POC between the DSW carbon isotope fractionation during the photosynthesis there and the cold intermediate water mass (Figure 2h). POC in [Nakatsuka et al., 1992]. This distinct difference in the d13C both water masses has a much higher d13C value (> 22%) of POC between the shelf and the pelagic areas may be than in pelagic waters, indicating that the POC in the cold useful in determining the origin of POC in the western intermediate water has actually come from the bottom of the region of the Sea of Okhotsk.
 Because the main area of sea ice production is the Sources of DOC and POC in Surface and wide continental shelf region along the Siberian coast Subsurface Waters [Alfultis and Martin, 1987; Kimura and Wakatsuchi,  There are usually two major sources for DOC and 2000] (Figure 1) and a strong anticlockwise current system POC in the area near large river mouths such as the present exists in the Sea of Okhotsk [Ohshima et al., 2002] study area. One is the in situ phytoplankton production. The (Figure 1), the DSW on the narrow shelf and the discharged other is the input of terrestrial organic matter from the river.
DSW found on the slope in Line-54N must have been Figures 5a and 5b show the relationships between DOC, transported from the continental shelf in the northwestern POC, and Chl-a concentrations in 0- to 200-m depths region of the Sea of Okhotsk. Water with DSW character- analyzed in this study, respectively. Although there is a istics does exist in the bottom layer on the shelf region clear linear relationship between POC and Chl-a (Figure 5b), northwestward of the Sakhalin Island (Figure 4). This water indicating that the major source of POC is the phytoplank- has the same physical and chemical characteristics as the ton production in this area, there are two different patterns DSW and the discharged DSW found on Line-54N.
in the distribution of DOC and Chl-a (Figure 5a), according  As for the surface water in Line-54N, the low- to the salinity range. In the high-salinity waters of more salinity water is distributed along the coast (Figure 2b), than 32 psu, there is a positive correlation between DOC and must have been discharged from the Amur River mouth and Chl-a, suggesting a contribution of phytoplankton to and transported beyond the northern end of the Sakhalin the in situ DOC production. However, we can also find Island. Because the strong western boundary current, namely another correlation between DOC and Chl-a with much the East Sakhalin Current, flows southward on Line-54N, larger DOC and smaller Chl-a concentrations in the low the low-salinity water is distributed being attached to the salinity waters of less than 32 psu, indicating the different coast. The low salinity reduces the density of this surface source of DOC, i.e., terrestrial organic matter input from the water mass (Figure 2c) and develops the water stratification NAKATSUKA ET AL.: DOC AND POC IN THE SEA OF OKHOTSK Relationship between Chl-a concentration and (a) DOC and (b) POC in the surface and subsurface waters (0 – 200 m) analyzed in this study. Solid and open circles in Figure 5a indicate thesamples with salinity ranges less and more than 32 psu, respectively. Solid and dashed lines in Figure 5ashow the linear regression of data with salinity ranges less and more than 32 psu, respectively. Solid linein Figure 5b indicates the linear regression of all the data.
 The Amur River water must affect the water mass in  In contrast to the DOC, the POC has a relatively weak the area around Station 86 because the water discharged correlation with salinity in the surface layer (Figure 7b). The from the Amur River first flows northward along the water collected near the Amur River mouth has the highest northwestern coast of Sakhalin Island before turning to POC value, however, and increases at the high-salinity the south beyond the northern end of the Island. Actually, range, too. The simultaneous increases of both POC and a very low-salinity water, of less than 20 psu, spreads over Chl-a near the river mouth (Figure 6c) suggest that marine this station (Figure 6). In the surface layer, DOC exceeds organisms must produce most of the POC in the western 300 mM, which is 3 times higher than that in the pelagic region of the Sea of Okhotsk.
surface water. In this water mass, POC is also very high.
 Because the Amur River water contains large amounts However, this increase in POC may not consist of POC of nutrients, especially silicate [Nakatsuka et al., 2004], the discharged from the Amur River, because d13C of the POC Amur River discharge must increase the productivity of is higher ( 20%) at this surface water than the typical d13C phytoplankton such as diatom in the Sea of Okhotsk. In fact, values of terrestrial C3 plants (usually less than the areas near the Amur river mouth and off the northeast [Sternberg et al., 1984], which are the dominant vegetation coast of Sakhalin are known to have the largest biological in the Amur River basin, and high POC concentration isaccompanied by a large amount of Chl-a, too, whichsuggests the occurrence of a phytoplankton bloom there.
Therefore the Amur River water is thought not to supplylarge amounts of POC into the Sea of Okhotsk, but ratherinduces a phytoplankton bloom through the input of majornutrients or micronutrients, although the DOC actuallyseems to be discharged from the river.
 The very good linear correlation between salinity and DOC in the surface layer in the study area (Figure 7a)provides important information about DOC in this region.
First, large amounts of DOC are supplied to the region fromthe Amur River. According to the y-intersection of theregression line, Amur River water contains 690 mM ofDOC. This value is much higher than the DOC of riverwater in temperate regions and is comparable to river waterin the polar region of northern Siberia [Lara et al., 1998].
Multiplying the annual amount of Amur River discharge(300 km3), 2.5 Tg/yr of terrestrial DOC is estimated to beexported into the northwestern region of the Sea ofOkhotsk. Second, the high linearity of the regression line(r = 0.99) indicates the conservative nature of the terrestrialDOC. Because conifer forests occupy the catchment area ofthe Amur River, the DOC in the river water should becomposed primarily of refractory humic substances origi-nating from forests [Spitzy and Leenheer, 1991]. Third,marine organisms in this region affect the DOC concentra- Vertical profiles of (a) temperature and salinity, tion in the surface layer to a very limited degree.
(b) DOC, (c) POC and Chl-a, and (d) d13C of POC at site 86.
NAKATSUKA ET AL.: DOC AND POC IN THE SEA OF OKHOTSK Relationship between salinity and (a) DOC and (b) POC in the surface layer (0 – 5 m) over the studied area. Solid line in Figure 7a indicates the linear regression of all the data.
productivity in the Sea of Okhotsk [Sorokin and Sorokin, which is equivalent to that of the DSW and the cold 1999; Saitoh et al., 1996], suggesting a direct effect from the intermediate water derived from the DSW, observed at Amur River water.
stations in the outer shelf and slope regions (bottom depthsare >100 m). There are strong negative correlations with Export of DOC and POC From the Shelf Bottom carbon, particularly with POC (Figure 8b), indicating that the to the Intermediate Water DSW that is rich in organic carbon is discharged from the  The high DOC and POC concentrations in the cold shelf to the slope area and mixed with the warmer pelagic intermediate layer attached to the slope (Figures 2e, 2f, 3e, intermediate water, which contains less organic carbon. The and 3f) suggest that a large amount of organic carbon is high linearity between the POC and temperature in the transported from the continental shelf to the ocean interior intermediate density range suggests that POC acts as a due to the DSW outflow, because a large volume of DSW on conservative component in the intermediate layer near the the shelf is actually transported outward from the shelf every slope and can be transported farther from the shelf edge into year by the East Sakhalin Current and/or as a density flow due the open sea. Because the living and/or very fresh POC are to a high density of the DSW itself [Mizuta et al., 2003; generally decomposed very quickly, the apparent conserva- Fukamachi et al., 2004]. The high d13C values of POC in the tive property of POC in the intermediate layer suggests the intermediate layer (Figures 2 and 3) indicate that most of the very fast transport of DSW into the intermediate layer on the POC transported into the intermediate layer was originally slope [Mizuta et al., 2003] and/or the nonliving and refrac- produced on the continental shelf by phytoplankton, although tory nature of POC in the intermediate layer probably we cannot estimate the proportion of marine and terrestrial originating from the sedimentary particles, which contain components in the DOC flowing into the intermediate layer highly degraded residues of marine organisms, on the shelf due to the lack of d13C data of DOC at present.
[Nakatsuka et al., 2002]. The fact that a significantly higher  Here we attempt to estimate the amount of organic concentration of Chl-a was detected at the intermediate layer carbon flux and discuss its implication for the biogeochem- on the slope (Figure 2g) supports the former process, but the ical cycle in the Sea of Okhotsk. Figure 8 shows the relation- ratio of Chl-a concentrations on the slope (approximately ships between the DOC and POC concentrations and 0.05 mg/L) to that on the shelf (0.5 – 1 mg/L) (Figure 2g) is the temperature in the density range from 26.7 to 27.0 sq, much smaller than the ratio of POC between the slope Relationship between the temperature and (a) DOC and (b) POC in a density range from 26.7 to 27.0 sq on the outer shelf and the slope areas, where the bottom depths are larger than 100 m. Solidlines indicate the linear regression of all the data.
NAKATSUKA ET AL.: DOC AND POC IN THE SEA OF OKHOTSK (approximately 2 mM) and the shelf (3 – 7 mM), suggestingthat the fresh POC consists of a small portion of total POCdischarged from the shelf to the slope region.
 If the temperature of DSW flowing out from the shelf 1.5C, the concentrations of DOC and POC in the DSW discharged from the shelf can be estimatedas 72.8 mM and 4.8 mM, respectively (Figure 8). Multiply-ing a previously reported flux of DSW outflow from theshelf to the intermediate layer (0.5 Sv) [Itoh et al., 2003;Gladyshev et al., 2000], we can estimate the annual flux ofthe DOC and POC from the shelf to the ocean interior in theSea of Okhotsk as 13.6 TgC and 0.9 TgC, respectively.
 In order to clarify the potential influence of these DOC and POC fluxes for the biogeochemical cycle in theocean interior in the Sea of Okhotsk, we try to comparethose fluxes with that of sinking POC flux measured by thesediment trap experiments [Nakatsuka et al., 2004]. Foursediment traps were moored at two sites, which werelocated approximately 150 km offshore from the northeastcoast of the Sakhalin Island at 54N and 49.5N, respec-tively. At both sites, one of the two sediment traps mooredcloser to the bottom recorded the intermittent lateral input of Fluxes of organic carbon into the intermediate lithogenic particles, which originate from the DSW outflow layer off the east coast of Sakhalin Island. Inverted triangles [Nakatsuka et al., 2004]. Therefore the POC and DOC on the map show the positions of sediment trap measuring discharged from the shelf due to the DSW outflow must also the sinking POC flux [Nakatsuka et al., 2004].
spread over these sediment trap sites, although most of theexported DOC and POC appear to flow southward along thecontour lines under the influence of a western boundary  This rough calculation inevitably indicates that the current, namely the East Sakhalin Current. Here we assume DSW outflow must affect the biogeochemical cycle in that most of the POC exported with the DSW are deposited the western region of the Sea of Okhotsk, particularly the or decomposed in an area off the east coast of north heterotrophic organisms in the intermediate layer of this Sakhalin (from 55N to 49N and within 300 km of the region. Sorokin and Sorokin  found an extraordinarily coastal line), and calculate the budget of organic carbon in abundant microbial biomass in the intermediate layer of this the intermediate layer of this area.
area. Nimmergut and Abelmann  also reported the  Because the area is 180,000 km2 and the sinking existence of a unique assemblage and highly populated POC flux monitored at the upper trap depth (260 – 280 m) of biomass of radiolarian, a kind of zooplankton, in the the two stations were from 1.1 to 2.7 gC/m2/yr, the annual intermediate water depth in this area. The POC and DOC load of sinking POC from the surface water to the interme- export accompanied with the DSW outflow from the shelf to diate layer can be calculated as 0.2 – 0.5 TgC/yr (Figure 9).
the intermediate water can explain the unique characteristics These values are much smaller than the lateral DOC and of heterotrophy in the intermediate water of the Sea of POC fluxes of 13.6 TgC/yr and 0.9 TgC/yr into the Okhotsk. Because the same types of dense water outflow intermediate layer of this area from the northwestern con- from the shelf to the ocean interior exist in seasonally ice- tinental shelf (Figure 9). Of course, parts of the DOC from covered areas all over the world, the accompanying organic the shelf must have already become refractory when dis- matter transport may also affect the intermediate water charged with the DSW, and most of the DOC may pass ecosystem in the world oceans.
through the intermediate layer of the area off Sakhalin  The discharged DSW is transported southward along without being consumed by intermediate dwelling orga- the intermediate layer of the Sea of Okhotsk, and finally nisms. However, Figure 8a shows that there is an approx- flows out into Pacific Ocean through Bussol' Strait in Kuril imately 10 mM difference in DOC concentrations between archipelago. This intermediate water mass is further trans- the DSW and the pelagic intermediate waters. Therefore we ported southward on the southeast of Kuril archipelago and infer that in the total DOC outflow of 13.6 Tg/yr, the Hokkaido Island of northern Japan, and joins to the forma- fraction that can be consumed in the intermediate water of tion of the NPIW at the region off northeastern Japan this area is approximately 2 Tg/yr, which is nevertheless [Yasuda et al., 1996; Talley, 1997]. Therefore the injection much higher than the sinking POC flux from the surface of a large amount of DOC in the northwestern region of the layer in this area (Figure 9). In the Sea of Okhotsk, primary Sea of Okhotsk may finally cause the increase in DOC in production is highest on the northwestern continental shelf the NPIW. This possibility has been suggested in a previous region [Saitoh et al., 1996], probably due to the river water study of the Pacific Ocean [Hansell et al., 2002], which input and the effective nutrient recovery from the shallow discussed the reason for the westward decrease in the 14C water bottom. The high productivity on the shelf, therefore, ages of DOC in NPIW [Bauer and Druffel, 1998]. If the can support the lateral supply of large amounts of organic organic carbon discharged from the northwest continental matter into the intermediate layer of the adjacent pelagic shelf in the Sea of Okhotsk actually increases the DOC in region through the DSW outflow.
NPIW, then the organic carbon must have a great impact on NAKATSUKA ET AL.: DOC AND POC IN THE SEA OF OKHOTSK biogeochemical cycles not only in the Sea of Okhotsk but Gladyshev, S., S. Martin, S. Riser, and A. Figurkin (2000), Dense water also in the wider area of the North Pacific Ocean.
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Temperature Science, Hokkaido University, N19 W8, Kita-ku, Sapporo Fukamachi, Y., G. Mizuta, K. I. Ohshima, L. D. Talley, S. C. Riser, and 060-0819, Japan. (email@example.com; nakatuka@lowtem.
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University, N10 W5, Kita-ku, Sapporo 060-0810, Japan.
Case Study Dr. Tabitha Ndungu presented to NACADA on their 2nd Conference in Nairobi, Kenya Date; 10th - 14th JUNE 2013 Venue: Moi Sports Centre Kasarani Gymnasium Theme: " The Youth and Drugs: A Call to Action." In spite of the damage done by
The International Journal Of Humanities & Social Studies (ISSN 2321 - 9203) www.theijhss.com THE INTERNATIONAL JOURNAL OF HUMANITIES & SOCIAL STUDIES Sacred Power of Menstruation versus Cultural Myths: An Interdisciplinary Overview Bhumika Sharma Assistant Professor, LR Group of Institutes, Solan, HP, India