International Journal of and Vol. 9 No. 2 December 2012:128-139

COASTAL UNDER THE INFLUENCE OF WESTERLY BURST IN THE NORTH OF PAPUA , WESTERN PACIFIC

Harold J.D.Waas1*, Vincentius P. Siregar2§, Indra Jaya2, and Jonson Lumban Gaol2 1Marine Study Program, Faculty of and Sciences, Pattimura University, Ambon 2Marine Science and Technology Departement, Faculty of Fisheries and Marine Science, Bogor Algicultural University, Bogor *E-mail: [email protected]; §E-mail: [email protected]

Abstract. Coastal upwelling play an important role in biological productivity and the in the . This research aimed to examine the phenomenon of coastal upwelling that occur in the coastal north of Papua continent under the influence of Westerly Wind Burst(WWB) prior to the development of El Nino in the Pacific. Data consisted of surface , vertical oceanic temperature, ocean color satellite image, wind and vector wind speed image, sea surface high, and Nino 3.4 index. Coastal upwelling events in the northern coastal waters of Papua continent occurred in response to westerly and westerly wind burst (WWBs) during December to March characterizing by low (SST) (25 - 28C), negative sea surface high deviation and blooming, except during pre-development of the El Nino 2006/2007 where weak upwelling followed by positive sea surface high deviation. Strong coastal upwelling occurred during two WWBs in December and March1996/1997 with maximum wind speed in March produced a strong El Nino 1997/1998. Upwelling generally occurred along coastal waters of Jayapura to Papua New Guinea with more intensive in coastal waters north of Papua New Guinea indicated by Ekman and depth maximum.

Keywords: Coastal upwelling, wind burst, El Nino, , Ekman layer Depth.

1 INTRODUCTION This role is shown by the ability of warm Upwelling is an event of raising pool (oligotropic) as the main area of the from the deeper to the surface world catch particularly both Skipjack waters that is mainly caused by the wind and Yellowfin tuna. This capability is blowing at a certain period. The ecological powered by contribution of north equatorial effects of upwelling are quite diverse, but cunter current (NECC) carrying water two impacts are especially noteworthy. First, upwelling rich in nutrients and chlorophyll-a upwelling brings up cold, nutrient-rich from Halmahera, Banda, Seram, and Sulu waters to the surface, which encourage (Messie and Radenac, 2006 ; Christian growth and support blooms of et al., 2004), eddys mechanism (Ganachaud phytoplankton. Second, the phytoplankton et al.,2011), high primary productivity from blooms form the ultimate base for coastal waters in Papua continent through the larger animal populations in higher food mechanism of seasonal current (NGCC and chain, including , marine mammals, and NGCUC), and Ekman transport caused by (Mann and Lazier, 2006). westerly wind burst (WWBs) (Kuroda, 2000; Upwelling that occurs in coastal waters Ueki et al., 2003; Lehodey et al., 2011). or coastal upwelling play an important role WWBs is a synoptic scale disturbances in biological productivity, the carbon cycle represented by strong westerly winds near in the ocean, and associated with productive the with a speed of more than 4 ms-1 areas. Although its account at a certain period and usually occurs during for only one percent of the ocean surface, the period from December to March. WWBs they contribute roughly 50 percent of the formed some mechanisms including intense world's fisheries landings (Vargas and tropical cyclone to jump in the cold of mid- Gonzalez, 2004; Mann and Lazier, 2006). and Madden - Julian oscillation

128 @Indonesian National Institute of Aeronautics and Space (LAPAN)

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(MJO) or their combination (Seiki and image; sea surface high deviation merge Takayabu, 2006; Tziperman and Yu, 2006). satellite ERS-2; Topex/Poseidon and GFO WWBs has been known to cause a shift image; data sets Nino 3.4 index ( 5S- warm pool to the east that is manifested in 5N; 170W-120W) and zonal wind velocity the form of equatorial Kelvin waves components of the cross-calibrated multi- produced depression, strengthen platform ocean surface wind vector L3.5 a ENSO in the eastern Pacific, activate the monthly first-look analyses data sets. Rossby waves propagate westward, and SST derived from satellite image was generate shallowing thermocline (new validated using SST insitu recorded by ten upwelling) in western Pacific (Tomczak and station (TAO) in western Pasific Godfrey, 2003; McPhaden and Yu, 2012; ocean at the same time to the date coverage McPhaden et al., 2011). of the image. Coastal upwelling research in northern The relationship between the incidence Papua Continent was published by of westerly winds and anomalies to the Hasegawa et al. (2009) and Hasegawa et al. development of El Nino in the Pacific (2010) which focused on the waters around established using the compilation graphs Papua New Guinea using hind cast zonal westerly wind component with Nino experiment with a high-resolution ocean 3.4 index using the microsoft Excel. El Nino general circulation models. However, with events indicated by the distribution of index the advances of remote sensing technology values greater than the threshold ± 0.4 C and the availability of satellite and in situ (http://www.cgd.ucar.edu/cas/catalog). oceanographic data (TAO and Distribution of SST, chlorophyll-a, sea Drifter), the study of coastal upwelling surface high deviation were compiled by events can be done in an unlimited time and using the interactive "Live Access Server" covers a broad region. This research aims to via the website http://coastwatch.pfel.noaa. examine the phenomenon of coastal gov/coastwatch/ and http://thredds.jpl.nasa. upwelling events that occur in the coastal gov/welding/getUI.do. waters north of Papua continent under the Upwelling events identified in the SST influence of WWBs prior to the development image (both Pathfinder and G1SST) tested of El Nino in the Pacific. by making vertical transects perpendicular coastline to latitude 1N, the vertical 2 MATERIALS AND METHODS distribution of temperature at position 138 E The research was conducted in the (1.5S - 1N) and 142 E (2.5S - 1N) using coastal waters northern of Papua continent recording data ARGO Drifter, and analyzed region with coverage area limited to 10S - using Global software Argo Marine Atlas. 10N; 125E - 155 E on March-September Upwelling velocity was determined by the 2012 (Figure 1). Data used in this study movement of isotherm 28C and 26C with include SST in situ data collected by simple equation: Mooring and accessed via …………………….. (1) http://www.pmel.noaa.gov/tao/; vertical temperature in situ data recorded by ARGO where: -1 drifter; monthly data sets of SST images in Vup= upwelling velocity (m.s ) 1996/1997, 2001/2002, 2005/2006 x = isotherm depth changes (m) (Pathfinder version day and night 4 Km t = change of time (s) spatial resolution ); SST G1SST Ultra - High Suitability analysis of the upwelling Resolution 1 Km (accuracy 0.001C/1 Km) location also tested using the calculation of (only Year 2013); ocean color satellite the Ekman transport and Ekman layer depth image; (zonal component) and utilizing the wind component parallel to the vector wind speed QuicSCAT satellite from the QuikSCAT satellite image

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Harold J.D. Waas et al. grid 2x2. Calculation Ekman transport and Ekman transport calculation results Ekman depth refers to the Pond and Pickard converted into Svedrup units where 1 Sv = (1983) with the form of the equation: 108 m3s-1

……………………. (2) where: M = Ekman transport (kg.s-1.m-1) yE x = wind stress component parallel to the coast (Pa) where: -1 DE= Ekman layer depth (m) f = parameter (rad.s ) . -1 = speed of earth's rotation axis (7.29 x W = wind modulus (m s ) obtained from 10-5 rad.s-1) wind strees image (QuickSCAT = latitude satellite) = latitude

Figure 1. Research location map (discription : = TRITON ; = Cross-Calibrated Multi-Platform Ocean Surface Wind ;TR = Transect (ARGO Drifter data) = Grid 2 x 2 ; = Nino 3.4 Region

3 RESULTS AND DISCUSSION T-test at the 95% confidence interval 3.1 SST Validation using a 2-tailed test at significance value of SST validation was performed on 50 0.173 was obtained tcal

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Figure 2 Relationship between SST derived from image and measured by Triton Bouy Mooring (TBM). Mooring (SST TBM)

Table 1. The results of statistical test (t-test) NOAA-AVHRR SST image with SST recordings by Triton Bouy Mooring in Western .

Paired differences T df Sig (2 Mean Std. Std. 95% conf. tailled) dev error interval diff. lower upper Pair SSTTBM vs SST -0.098 0.505 0.071 -0.242 0.044 -1.383 49 0.173 CST

3.1 Westerly wind burst (WWBs) occurred in December. El Nino in 2006/2007 and El Nino produced without the presence of WWBs at The time series distribution of zonal speeds ranging from 1.1 - 2.7 ms-1 where the wind component and Nino 3.4 index in peak maximum velocity occurred during Figure 3 proved that the variability of December. WWBs influence the duration and intensity WWBs is defined as the event winds of El Nino events. The development of El with speeds greater than 4 ms-1 and lasted at Nino in 1997/1998 due to WWBs that least a few days (5-40 days) and occurs in occurred in December and March response to some external such as 1996/1997. Wind speeds ranged from 2.84 - Madden - Julian ocillator (MJO) or tropical 5.72 ms-1 with a maximum speed occurred cyclone intense (Seiki and Takabayu, 2006; during the month of March. Meanwhile, El Tziperman and Yu, 2006). El Nino events Nino in 2002/2003 produced by WWBs that which took place in the East Pacific and occurred in December and March 2001/2002 coastal upwelling in the north coast of Papua with wind speeds ranging between 2.84 – New Guinea variability was significantly 5.34 ms-1 where the maximum speed WWBs associated with the incidence of variability

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WWBs (Helber and Weisberg, 2001; classified into stronger intensity in McPhaden, 2004; Hasegawa et al., 2010). 1997/1998, moderate intensity in 2002/2003, The influence of WWBs to the and the weak intensity 2006/2007. This development of El Nino in the Pacific also criterion is identical to the pattern of events shown clearly on the distribution of index which WWBs strong El Nino events are Nino 3.4 (Figure 3). By using a threshold of characterized by two peaks WWBs with ± 0.4 C, the threshold value Nino 3.4 SST maximum speed on the latest event (March), index then can be found the influence of with a moderate El Nino events WWBs two WWBs during the 1996/1997. El Nino peaks but the peak incidence of both lower took place for 14 months (April 1997 - May speeds (March), while the weak El Nino is 1998) with maximum intensity during not followed by events WWBs but zonal October-November 1997. WWBs during westerly wind maximum speed greater than 2001/2002 induce El Nino events over the 2 ms-1. From these results, the distribution of past12 months (April 2002 - March 2003) the zonal wind component at speeds greater with a maximum intensity occurred during than 2 ms-1 was used as a speed preference November-December, while the west wind west monsoon that will trigger El Nino with events without the presence WWBs weak intensity, while WWBs presence at 2005/2006 El Nino lasted for 8 months (June speeds greather than 4 ms-1 was significantly 2006 - January 2007) with maximum generate events El Nino with a moderate to intensity also occurred during November - strong intensity, depends on wind speed and December but its strength was weaker than duration of events as described by the the previous two years of El Nino. distribution index Nino 3.4 (Figure 3). Based on criteria of Oceanic Nino Index refers to the third years, El Nino are

Figure 3. Zonal wind component and Nino 3.4 index during El Nino years (1997/1998, 2002/2003,2006/2007)positive = westerly wind , negative = easterly wind. Index Nino 3.4 positive = El Nino.negative = La Nina, dashed line is the threshold ± 0.4C

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3.2 Coastal upwelling characterized by sea surface Coastal upwelling in the year of range 27 - 28C at north of Papua New 1996/1997 was preceded by the presence of Guinea coastal waters (Figure 4, 5, and 6). WWBs (December and March). Coastal During the WWBs, coastal upwelling upwelling beginning to grow in December, occurred in coastal waters northern of Papua was characterized by low sea surface continent and triggered El Nino events in the temperatures in the eastern of and Pacific (Ueki et al., 2003; Hasegawa et al., northern of Halmahera Island. Along with 2009; Hasegawa et al., 2010). This the intensification of the WWBs, SST was statement supported by the results of lower than normal conditions in the north of previous analyses of the zonal wind Waigeo Island, Manokwari and Biak Island component (U) and the Nino 4.3 index surrounding waters to the east ofcontinent. suggesting that the variability WWBs in the Strong coastal upwelling clearly visible western Pacific significantly affect the during March where SST ranges 26 – 27C strength of El Nino events that occurred in was concentrated in the coastal waters the eastern Pacific in three events with between Jayapura - Papua New Guinea different intensity. This indication signaled (138°E - 149°E) and corresponding to the that the incidence of coastal upwelling in wind speed greater than 5 ms-1 parallel to the coastal waters northern of Papua continent coastline. The location of the coastline will be comparable with the intensity of El forming an angle ( ) 22.5 (Hasegawa et al., Nino which to be generated. 2010) and the influence of the wind strees Coastal upwelling due to Ekman adn , produced Ekman transport of surface water moving away transport move surface water away from the from the coast while the void surface water coast and piled up on the equator. In the year was replaced by water from deeper layers of 2001/2002, WWBs produce coastal with lower temperatures. When the wind upwelling with sea surface temperature was parallel to the coastline in the surface, range similar but the intensity was not as Ekman transport directed 90 to the right strong as 1996/1997 period. In the year of (left) of the wind direction in south (north) 2005/2006, there was no presence of of the equator, resulting in movement of WWBs, and weak coastal upwelling surface water off the coast in the direction of

Figure 4 Satellite image of SST , chlorophyll-a and sea surface high deviation during period of westerly wind and WWBs (December – March) 1996/1997. International Journal of Remote Sensing and Earth Sciences Vol. 9 No.2 December 2012 133

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Figure 6. Satellite image of SST, chlorophyl-aandSea surface high deviation during period of westerly wind and WWBs (December – March) 2005/2006. the two parts of the hemisphere. detection both Pathfinder and G1SST ultra - Consequently, coastal upwelling decrease high resolution, coastal upwelling events in near the coast. The consequence the coastal waters north of Papua continent was a gradient normal to the coast, was characterized by sea surface temperature which encourages geostrophic currents along preference 25-28C under the influence of westerly winds and WWBs (Figure 7). the the coast with the same direction of Coastal upwelling is also characterized movement by the wind. Net movement of by low sea surface high deviation and water was the result of Ekman flow blooming phytoplankton which is marked by generated by wind and increased concentrations of chlorophyll-a in flow. It was directed away from the the waters. It can be understood because near the surface, parallel to the coast at mid- these three parameters interact each other depth and at an angle that to the coast where the thermocline shallowing indicated in the bottom waters (Tomzcak and Godfrey, by the low dynamic height associated with 2001). negative value of sea surface high deviation. SST as the main indicator of upwelling Simultaneously, nutrient-rich cold water events was also detected using SST imagery from the thermocline can reach surface G1SST ultra - high resolution over a period waters due to barrier layer disappears of westerly winds and WWBs in 2012/2013 triggering phytoplankton blooming. During (December-March). The analysis showed the westerly wind burst period (1996/1997 & similarities of the of upwelling events in 2001/2002) upwellling was characterized by coastal water of Manokwari - Biak to about negative value of sea surface high deviation 138 E during January-February with the distribution pattern of curving (SST 24- 27C) while in March, upwelling northwest towards coastal waters north of dominates the coastal waters around Papua continent, especially in the waters of Jayapura - Papua New Guinea (SST 25 - the main central upwelling events. 27C). Based on the result of image Moreover, this pattern also had similarities

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Coastal Upwelling under the Influence of Westerly Wind Burst ... with the pattern of distribution shown by the Phytoplankton blooming that occurred distribution of wind speed and wind during WWBs had the same general pattern, direction vector. This indicated that a strong where high chlorophyll-a concentration wind strees during WWBs able to move the corresponding to the low sea surface surface water and the vacuum is temperatures as on record by OCTS and replaced by water from the layer below it so SeaWiFS satellite imagery in January-March that decreasing surface temperature and sea 1997 & 2002. Blooming concentrated in the level. Another factor contributing to decrease waters around Biak island, Jayapura - Papua of sea level during this period coincideed New Guinea coastal waters and the with the arrival of partly phase of Rossby coincided with the low sea waves on north branching of 5 - surface temperatures. Unlike the previous 7N which hit the east coast of Mindanao period, during weak upwelling, island on Phillipina and reflection following phytoplankton bloom also occurred on the distribution pattern of the wind to the coastal waters. Besides to coincide with low coastal waters north of continent. The SST, blooming occurred due to nutrient-rich presence of equatorial on the water from the coastal area on injection to waters part as a response to a shift Warm equator through mechanism anomalies new Pool to the east that occurred during the guinea coastal current (NGCC) on surface WWBs. These waves caused disturbances in waters and new guinea coastal under current the thermocline and Sea Level (Tomczak and (NGCUC, in the thermocline) reverse Godfrey, 2003). Different condition was direction to the southeast along coast north shown during an episode in 2005/2006 years of continent and turn direction around where the weak upwelling followed positive longitude 142E, which seem obvious in the value of sea surface high deviation. This was pattern of chlorophyll-a distribution on due to the absence of WWBs so the shoaling ocean color imagery, and joining with Warm Pool to the east was weak. As a result equatorial under current (EUC) (Kuroda, the equatorial Rossby wave generated very 2000; Ueki et al., 2003). NGCC together weak compared to the conditions pre strong and moderate El Nino.

Figure 7 Satellite image of SST (Ultra – High Resolution) coverage of the period December– March 2012/2013.

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Harold J.D. Waas et al. with cold water as the result of Ekman also reported by Hasegawa et al. (2009) and transport mechanism was directed and Hasegawa et al. (2010) by using CTD accumulate at the equator, while NGCU recordings by RV/Kaiyo in September 2000 joined the EUC to inject higher and December 2001 at the same location concentration of (Fe) from Papua New (142 E). In normal conditions the isotherm Guinea coastal waters (Sepik ) to limit 28C is found at a depth of 50 - 55 m, in the on the central Pacific event of WWBs the isotherm at the depth of (Lehodey et al., 2011; Ganachaud et al., 30 - 40 m. Similarly, the 27 C isotherm at 2011). normal conditions ranged between 60 - 70 m, The presence of coastal upwelling and while upwelling events at depth 45-50 m or the loss of barrier layer during the period of upwelling intensity stronger than normal WWBs increase primary productivity, and conditions (Figure 8). warm pool become fishing grounds and Characteristics that have been identified spawning ground (high recruitment) of as SST, sea surface high deviation and Skipjack tuna. This mechanism was part of chlorophyll-a concentrations needs to be the enrichment process of the oligotrophic tested by the Ekman transport and Ekman warm pool besides chlorophyll-a front layer depth calculations extracted from (Figure 4 and Figure 5) and eddies that QuikSCAST satellite image data at the same existed during the period of development of coverage period. The calculation results the westerly wind and WWBs in 1996/1997, showed that the westerly wind and WWBs 2001/2002, and 2005/2006 in the NECC move the water masses on zonal 1N along flows among Phillipina - Indonesia - Papua the longitude 131E - 135E leads to the New Guinea. coast, while at the zonal between 1S - 3S Coastal upwelling phenomena detected along longitude 137 E - 149 E the water by satellite imagery verified by Drifter mass moved away from the coast as an ARGO data analysis during the December to indication of upwelling events. Areas along March 2008/2009 (data available from 2004 the coast between longitude 140E - 149E - 2012), period of the early development of (Jayapura - Papua New Guinea) was a region the moderate El Nino 2009/2010. The results of potential occurrence of upwelling due to showed that along the transect TR1 at the strategic location to the wind trajectory. longitude 138E (1.5S-1N) during westerly This evidence caused the cold water move winds and WWB (wind speed 1 - 4 ms-1) away from the coast more intensive which upwelling occurred near the southern coast indicated by the higher value of the Ekman of 1.2 S, indicated by an increasing the transport (0.01 – 0.20 Sv) from other parts of isotherm 28C from depth of 85 m the coastal waters (Figure 9). (December), 60 m (February) with upwelling -4 -1 Similar indication was also shown by velocity 4.8 x10 cm.s . Similarly, the 26  the calculation result of the Ekman layer C isotherm upward from the depths of 117 - -4 -1 depth. On the most potential coastal 95 m with velocity 8.5 x 10 cm.s . upwelling region, Ekman layer depth was Meanwhile, a similar trend occurred in TR2 relatively deeper (38 – 85 m) generated by transect at longitude 142 E(2.5S - 1N) WWBs with speed 4.79 – 7.42 ms-1. where upwelling occurred in the south Meanwhile, on the others coastal upwelling longitude 2.5S indicated by the move-up of region, Ekman layer depth was relatively 28 C isotherm near the coast of Papua New shallow (20 – 29 m) generated by WWBs Guinea from depth of 85 m (December) - 65 with speed 4.12 – 6.25 ms-1 (Figure 10). By m (February) with the velocity of 3.8 x 10-4 comparing depth distribution of normal cm.s-1 while the 26C isotherm going up isoterm 27C and 28C during 2000/01 and from the depth of 115 m (December) - 105 m moderate El Nino 2002/03 with Ekman layer (January) with velocity 3.5 x 10-4 cm.s-1. depth calculation result , it can be speculated Evidence of coastal upwelling events were that wind stress cause by WWBs in the

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(a) (b)

Area of upwelling events indicated by satellite imagery based on specific

Figure 8 . Vertical distribution of temperature (a) ARGO Drifterrecordings along longitude 138°E & 142 °E; (b) CTD RV/Kaiyo recordingalong longitude 142°E (Hasegawa et al.,2009 & Hasegawa et al.,2010).

Figure 9. Ekman transport distribution on a grid 2x 2 in coastal waters north of Papua continent.

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Figure 10. Ekman transport distribution on a grid 2x 2 in coastal waters north of Papua continent. region between Jayapura – Papua New moved away from the coast and deeper water Guinea produce coastal upwelling with SST column influenced by wind stress. In range 27 – 28 C corresponding to the range addition to winds, coastal upwelling caused of SST found by Hasegawa et al.(2009) ; by advection of equatorial Rossby waves in Hasegawa et al. (2010) and Leger et al. response to movement of Warm Pool to (2010) using NOAA/AVHRR satellite SST eastern Pacific and NECC & NGCUC the image and CTD data during coastal reverse direction to the southeast at around upwelling event in this region. Coastal longitude 142E (anomalie) together with upwelling with lower SST could be expected Ekman transport water mass leads and to occur during strong El Nino conditions hoards nutrient-rich water mass and where the wind stress generated by WWBs -1 chlorophyll-a at the equator. with speed > 7.5 ms . ACKNOWLEDGMENTS 4 CONCLUSION The research was carried out with the Under the influence of westerly winds aid of SEAMEO BIOTROP through Grants burst (WWBs), an intensive coastal DIPA 2012. We would like to thank upwelling (moderate and strong intensity) occurred with winds speed more than 4 ms-1. International Agency such as NASA JPL, Meanwhile, weak upwelling occurred PO.DAAC, NOAA, TAO (Tropical without the presence of the westerly wind Atmosphare Oceanic Project), and ARGOS burst with wind speed greater than 2 ms-1, providing satellite imagery data and which took place from December to March oceanography data of western Pacific ocean and could be used as an indicator of the through Live Access Server (LAS). We also development of El Nino in Pacific. Coastal would like aknowledge the Laboratory of upwelling indicted by low SST associated Remote Sensing and Ecology SEAMEO with negative value of sea surface high BIOTROP (Petrus Siregar, and special deviation and phytoplankton blooming, thanks to J. Situmorang & Mrs. Juliani for except in 2006/2007 period that weak administration support). upwelling accompanied by positive value of REFERENCES sea surface high deviation. The coastal waters north of Jayapura (Irian Jaya) – Papua Christian, J.R, R. Murtugudde, J. Ballabrera- New Guinea are potential areas of upwelling. Poy, C.R. McClain, 2004, A ribbon of However the coastal waters North of Papua dark water: phytoplankton blooms in the meanders of the Pasific North New Guinea is the place of occurrence of strong intensity, which characterised by the Equatorial Counter current, Deep-Sea magnitude of the mass transport of water that Research II, 51:209 - 228.

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