Paleo-latitude of the Intertropical Convergence Zone in the Northeast Pacific during Late Cenozoic

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(1)Vol. 26(2):245-253. Ocean and Polar Research. June 2004. Article. & ê8 §ÿï· æ ê>Z&~ *~æz ;89ÁB8*ÁæçºÁ.4"* ·ö &~ãÁ¶ö¦ (425-600) ãVê nÖ nÖÖÚ ÒB 29^. Paleo-latitude of the Intertropical Convergence Zone in the Northeast Pacific during Late Cenozoic Kiseong Hyeong, Ki-Hyune Kim, Sang-Bum Chi, and Chan/ Min Yoo* Marine Geoenvironment and Resources Research Division, KORDI Ansan P.O. Box 29, Seoul 425-600, Korea. Abstract : The Intertropical Convergence Zone (ITCZ), where the southeast and northeast trade winds converge, is the effective climatological barrier that separates the southern and northern hemispheres in dust budget. Asian and N. American dusts dominate in the Pacific north of the ITCZ, while Central and S. American dust prevails south of the ITCZ. In order to understand the nature of latitudinal and depth-related variations of mineral composition in terms of relative position to the ITCZ, deep-sea core sediments were collected from 9oN to 17oN at a 2o interval along the 131.5oW meridian and analyzed for mineral composition. The amount of illite in surface sediments decreases gradually from 65% at 17oN to 31% at 9oN. In contrast, smectite increases from 11% to 56% southward. The observed mineralogical variation toward the ITCZ is attributed to the increased supply of volcaniclastic material transported via the southeast trade winds from the Central and South America source regions. Smectite-illite transition, a phenomenon that the amount of smectite increases over illite, occurs at around 10oN, the northern margin of the ITCZ. This result indicates that the change in latitudinal position of the ITCZ in geologic past could be recorded as a form of smectite-illite transition in deep-sea cores. The studied cores show down-core variation of mineral composition from illite-rich at the surface to smectite-rich clay suit at depths, similar to the latitudinal variation. The smectite-illite transitions observed in these cores are likely the records of changes in latitudinal position of the ITCZ. The depth and age of smectite-illite transition is getting shallower and younger toward equator, implying that the ITCZ was located farther north during late Tertiary and has shifted southward to the present position of 5oN-10oN. Key words : 'ê>Z&(ITCZ), §ÿï·(Northeast Pacific), & 'b(Deepsea sediment), 7b W(Mineral composition). 1. *. . & [ 'böº :²ö ~ ÿ>Ú 9 ^ ã~ ö·W 'b Ö^~² ª . 'b~ W Wª" «¶ V f &V~ B~ö &7 &N *Corresponding author. E-mail : [email protected]. ®b, 'b Ú >Ú ®º V f " &V B~j ~º Ö FÏ~² ÏB . ß®, Gçö B fÒ ÎÚ^ ®, bVö 'b~ · 'b, >~ vª ö ~ v¦·Ïj Aæ pf æ~ ' b~ ãÖöº &VB~ö ~ V ~ º. ~ 'Ë ·V r^ö ~ ö ' æb Îê ..

(2) 246. Hyeong, K. et al.. 'ê>Z&(Intertropical Convergence Zone, ITCZ)º ÎÿZ³" §ÿZ³ ò¾º bB 'êæ~ &VB~ ;¢ >'~º 7º Vê' º². (Pisias and Mix 1997). 'ê>Z&º ;Öï ¸j V 7~ bæ «¶¢ Î"'b BbB §>f Î > Vö~ bæ«¶& æb ÿ~º ©j N ~º OÚã j ~ ® (Rea 1994; Hovan 1995; Pettke et al. 2002). Ö", 'ê>Z&~ Î¦º ÎÿZ ³ö ~ Ò §¦º §ÿZ³ö ~ ÿ N «¶& Ö^~² '>º ©b rJ^ ® (Lyle et al. 2002). V¢B 'b VçöB §>f Î>~ Vö æ æz¢ æ > ® , ~ ¢ Û " æ î& ÿn 'ê>Z&~ *~¢ º; > ® . 'ê> Z&~ *~º §>f Î>~ &VB~ ; æzö V¢ " æî& ÿn *~& æ³'b æz zr rJ^ ® (Flohn 1981; Pettke et al. 2002; Lyle et al. 2002). *Ò ÿï· æöB 'ê>Z&~ *~ º ê.ö V¢ §ÿZ³" ÎÿZ³~ ç&' ^V & æzbB 5oN-10oN ÒöB Î§OËb ê³ æz~ ® (Pickard and Emery 1982). º §ÿï· æ 7 17oNöB 'ê>Z&~ §ã ãê 9oNræ~ *öB j & [ 'b~ *êê 7bW æzf 'ê>Z&~ ç&' * ~ Ò~ &ê¢ «~º Ï' ® . 6 7b W~ >ç' æz;f ['b~ *êê æz·ç j jvb, B3V ÿn 'ê>Z&~ ç&' *~ æzê º' ¶ ~& .. 2. æ B & >¯B æf §ÿï· ¢ÒN-Ò¢Ê &(C-C æ, Clarion-Clipperton fracture zone)~ 7 ö *~ &" *Z ëBB7 æ. (Fig. 1). >f Îã(5-6oN) æöB £ 4,000 m ;ê Ô² ¾æ¾, §b .> 66 Ã&~ 8oN ¦"ö Bº £ 5,000 m pÚê . ® ö ÏB "ç ò¢ j 8-17oN *öBº 4,800-5,100 m Ò¢ ¾ æÚ, *êö V >~ æz¢ æº pº. (·>Ö¦ 2003, 2004). C-C æ 7 Î¦ 5-6oN *f > Ô >[~ ÖK ¸j " êÖ" 7b WB 'b 310 mm/1000j ;ê '> ®b¾, §¦æöBº ö·W 6Æ& Ö^ 'b 1 mm/1000j ~ ç &'b Ôf 'Nj 9 ® (Piper and Williamson 1977; Müller and Mangini 1980; Halbach et al. 1988). ~æò, ; &[~~ 'Ëj Aº æöBº. Fig. 1. Site locations of samples used in this study. The full names of sampling stations are shown in Table 1. The boxed areas of K1 through K7 show the location of blocks allocated exclusively to Korea for manganese nodule exploration.. 'b~ " Ò' *ç ;~² ¾æ¾æ æ ö V 'N~ æz& Ö ² ¾æ¾Vê . (Piper and Blueford 1982). ò& jB 9oN §¦ ~ 'bf ê.ï 6º ².ï~ î ^ W >Ú ®b, 5 kg/m2 ç~ *Z& [ö ª~ ® (·>Ö¦ 2004).. 3. Òò 5 ª+ O» ® ö ÒÏB 'b òº 2003j · ö & ~ãöÒ(KODOS 03-03)öB "çòj V¢ Ï~ 131.5oW ãFj V¢ 9-17oN *öB 2o *Ïb 5B ;6öB j~& (Table 1, Fig. 1). PC 02-01-02 òº 2002j ·ö KODOS 02-01 öÒ 16o12'N, 125o59'WöB j~& (Table 1, Fig. 1). j òº FçöB >b .B ê zç~ ßW j ¶^® VÒ~ Òê¶ò¢ ³ Ê, ªCj * 1 cm *Ïb ¦ò¢ j~& . ¾^æ zjº thermal tube¢ Ï~ &/ ê ïË&~& . 'b~ *êÁêê WWª~ æz¢ rjÚV * ªöòö & X-F ².ªCj ~& . ªC j * *òf 6Æ7b ªÒòö & Phillips PW1710 X-F ².ªCV(40 kV/30 mA)¢ Ï~& ..

(3) 247. Paleo-latitude of the Intertropical Convergence Zone in the Northeast Pacific Table 1. Sampling locations and lengths of the studied cores, and water depth of sampling sites. Station number PC 03-03-N09 PC 03-03-N11 PC 03-03-N13 PC 03-03-N15 PC 02-01-02 PC 03-03-N17. (N9) (N11) (N13) (N15) (N16) (N17). Locations Latitude (N) Longitude (W) o 09 00' 131o30' 11o00' 131o30' 13o00' 131o30' o 15 00' 131o30' o 16 12' 125o59' 17o00' 131o30'. *òº 3o2θöB 60o2θræ~ ².¶ò¢ ³~&b , 6Æ7b ªÒòº 3o2θöB 30o2θræ~ ².¶ò ¢ ³~& . 6Æ7b ªCj *B âRï jV¢ Ï~ ;O*Þj B·~& . -² B· Z¾Ò ò Þö & ªC~, ÿ¢ Þö & ö 2&Ò¾Ò¢ ê ªCj ~& . *ò ªCj Û áf ¶òöB Schultz(1964)~ O »j Ï~ C', ËC, Ò C 6Æ7b~ ·j > ;ï'b êÖ~&b, 6Æ7b Wf Biscaye (1965)~ peak 'j êÖO»j Ï~ ².¶òö ¾æÂ Ê{æÞ, ¢¢Þ, RÒ¾Þ, îC ö & > ;ïªCj ~& . PC 02-01-02 ò~ ã Ööº jãÒÞ b& ¶RÒ¾Þ/îC(7.2 ç)f ËC(3.24 ç, 3.19 ç)~ "º bf ß~V r^ö jã ÒÞ& ô ª~º 250 cm ~¦öBº > ;ïªC ®&Ë~&b, V¢B 250 cm ç¦ òö &Bò > ;ïªCj ~& .. 4. Ö. . ªC ò~ 7bW" æ ¦"~ &*ê(811oN, 148-153oW8-11o)öB Vö >¯B Ö"¢ f âb >~& (Table 2; Figs. 2, 3; Jung et al. 1998). òº " C', ËC, Ê{æÞ, ¢¢Þ, îC, ¶RÒ¾Þ b W>, pf *êö V Úê' 7bç~ æz¢ (Table 2; Fig. 2). b& pö V 7bW~ æz·çj ÚÚ, C', Ë C, C 6Æ7b, ¶RÒ¾Þ~ ïf pö V « {~ ÛB æz¢ æ pº >, îC, ¢¢ Þf Ê{æÞ~ ·f pö V¢ ¢;~² Ã& 6º 6²~º ·çj (Table 2; Fig. 2). Î ò~ ['bf ¢¢Þ& 50% çb Ö^~, p& Ã&~B · 13%ræ 6²~º ãËj . > Ê{æÞº [öB · 11-27% ¢¢Þö j~ Ö 'æò, p~ Ã&ö V¢ 6N Ã&~. Water depth (m). Core length (cm). 4823 4884 4956 5029 4550 4741. 541 444 665 743 477 328. ¢; p ~öBº &Ë Ö^ ·j ¾æÞ (Fig. 2). Ê{æÞ& ¢¢Þ Ö^æº Ê{æÞ-¢¢ Þ *&~ pº ç&'b *êöB p &* êöBº »f ãËj . .¢ , 13-17o *ö B j ò~ ãÖöº 250-360 cm pöB Ê{æ Þ& ¢¢Þ Ö^æº >, 8-11oN *öB º æ&& [ 40 cm ÚöB ¾æÂ (Figs. 2, 3). .'b 11oNöB j PC 03-03-N11 òö Bº ªC ò 7 &Ë »f p 40 cm¦V Ê{æ Þ& 90% çb Ö Ö^ ãË (Fig. 2), Jung et al.(1998)ö ~ B GC90-26(9.5oN) "ç ò 6 [¦V Ê{æÞ& Ö^ ·çj ¾æÞ. (Fig. 3). º ò& jB v æ~ [ 'b ; Î&[>(AABW)ö ~ ¦ª' j Aj ¾ æÂ *ç ©b ê . Î&[>ö ~ & 'b~ ¦ª' " Ò' *çf æöB &V> ® (Johnson 1972; Piper and Blueford 1982; Skornyakova and Murdmaa 1992). 15oNöB j PC 03-03-N15öBº ò " Ò Ê{æÞ& Ö^ æº *&& &V>æ pº, º &[>ö ~ " Ò' *çö ~ æ' 'N~ Ã&ö ~ ©b CB . îCê ¢¢Þf FÒ~² [öB &Ë ³¦~ ~¦ &B 6²~º ãËj . ['b Ú~ Ê{æÞf ¢¢Þ~ ïf ò j ;6~ *êö V¢ æz~º ·çj (Fig. 4). *Ú'b &*ê .> Ê{æÞ~ · Ã&~ ¢¢Þ& 6²~º ãËj æò, ~9o30'N ÎöB º ¢¢Þ& Ã&~ Ê{æÞ~ · 6²~º > &>º ãË ¾æÂ (Fig. 4). ['b Ú ¢¢Þ ~ ·f 17oNöB 65% &8 ¾æ¾ 9o30'NöB º 31% &8 º >, Ê{æÞ~ ·f 17oNöB 11% &8j, 9o30'NöB 56% &8j ¾æÞ (Fig. 4). 16oN æöB j PC 02-01-02 òöBº ßû' b jãÒÞ& &VB . jãÒÞº ¢¢Þ&.

(4) 248. Hyeong, K. et al.. Ö^ ç¦öBº &V>æ p, ç&'b Ê{æ Þ& Ö^æº 250 cm ~öBò ª . 6 &¦. ª~ "çò öBº Ê{æÞ& Ö^ ¦ªöB 9 ç~ Ï¶*Ïj &æº 7b z® &V>º, º. Table 2. Mineral composition of the studied samples. Clay contents were normalized to 100%. PC 03-03-N9. PC 03-03-N11. PC 03-03-N13. Depth (cm) 1 40 80 120 160 200 240 280 320 360 400 440 480 520 540 1 40 80 120 160 200 240 280 320 360 400 440 1 40 80 120 160 200 240 280 320 360 400 440 480 520 560 600 640. Quartz 20 11 11 11 9 9 6 6 4 8 7 5 4 5 6 13 5 5 5 8 6 8 7 7 8 8 8 30 33 21 23 26 19 20 19 23 20 18 21 19 17 21 21 23. Plagioclase Total Clay 10 70 9 80 12 77 10 78 9 82 9 82 9 85 6 88 6 90 7 85 6 87 7 87 4 92 15 80 9 85 8 80 8 87 8 86 5 90 8 84 9 84 11 82 8 85 9 84 11 82 12 80 11 80 10 60 11 56 8 71 9 68 10 64 10 70 9 71 11 70 8 69 10 70 9 73 9 70 9 72 6 77 10 69 10 69 13 64. Smectite 27 69 66 65 70 58 76 83 87 75 69 69 74 80 n.d. n.d. 90 91 94 76 74 70 65 65 68 70 n.d. 23 25 24 28 35 34 40 42 36 43 47 50 52 53 56 54 54. Illite 52 23 24 25 22 31 19 14 8 15 23 20 18 13 n.d. n.d. 8 8 4 18 17 19 14 15 20 17 n.d. 54 57 58 54 51 49 45 44 46 42 39 37 34 35 33 32 34. Kaolinite 8 6 6 6 6 6 2 2 3 8 6 6 6 4 n.d. n.d. 2 1 2 4 5 9 17 9 7 5 n.d. 6 9 9 9 8 6 6 7 8 6 6 5 6 5 5 7 6. Chlorite 13 3 5 4 3 5 3 1 3 2 3 4 2 3 n.d. n.d. 1 2 3 3 4 10 5 8 n.d. 17 9 9 10 6 11 9 7 10 9 9 7 7 7 6 8 7.

(5) Paleo-latitude of the Intertropical Convergence Zone in the Northeast Pacific. 249. Table 2. Continued. PC03-03-N15. PC 03-03-N17. PC 02-01-02. Depth (cm) 1 40 80 120 160 200 240 280 320 360 400 440 480 520 560 600 640 680 720 1 40 80 120 160 200 240 280 320 360 400 440 1 50 100 150 200 230 245 250 255 260 265 270 275 290 300 310 320 328. Quartz 22 26 20 21 21 19 19 21 19 18 18 18 19 20 18 20 19 19 19 32 21 24 32 22 21 24 16 23 20 17 16 21 20 19 15 21 19 17 16. Plagioclase Total Clay 10 68 8 66 8 72 7 73 8 71 9 72 8 73 8 70 9 72 8 74 9 74 7 75 8 73 10 70 10 72 8 72 9 72 7 73 8 73 12 57 10 69 10 66 13 55 10 67 11 67 11 65 11 73 14 63 13 67 12 71 14 70 7 72 8 72 9 72 11 74 9 70 10 71 11 72 13 71. Smectite 17 21 14 19 20 29 29 24 24 32 32 30 33 28 36 38 30 40 29 11 15 16 24 25 35 40 43 44 44 48 51 20 19 23 25 31 30 n.d. n.d. 66 55 63 60 76 69 67 63 65 66. Illite 58 58 63 62 60 53 53 56 59 54 52 53 52 54 51 50 56 50 54 65 60 62 57 56 47 42 39 39 39 36 34 55 57 55 53 47 50 n.d. n.d. 34 45 37 40 24 31 33 37 35 34. For the samples below 250 cm depth of PC 02-01-02, smectite and illite contents were normalized to 100% (see Methodology section for details).. Kaolinite 8 8 10 9 8 8 6 9 6 7 6 7 7 12 6 6 6 6 6 9 7 8 7 7 7 8 8 7 8 9 8 7 10 7 7 9 9 n.d. n.d.. Chlorite 17 14 13 10 12 10 12 11 11 8 9 10 9 7 7 5 8 5 10 15 18 14 11 12 10 11 10 10 9 6 8 17 14 15 15 13 11 n.d. n.d..

(6) 250. Hyeong, K. et al.. Fig. 2. Down-core variations of smectite and illite in the studied cores. The amounts of smectite and illite in PC 02-0102 (N16) were normalized to 100% due to the occurrence of phillipsite that prevents quantitative estimation of kaolinite, chlorite, and feldspar (see methodology section for details). Horizonal lines represent the depth of smectite-illite transition.. Fig. 3. Down-core variations of smectite and illite in the cores from 8-11oN, south of the studied cores. Data are from Jung et al. (1998). Horizonal lines represent the depth of smectite-illite transition.. æîB zÖêJW 'böB z® &V>º Ò¯ ¢Þ ©b Îê (e.g., Aoki and Kohyama 1998).. 5. Æ. ~. *êê %b`9 æz §ÿï· & 'bö ª~º Ê{æÞ~ V öj C®Jº & ô ê¯>Ú zæò jçræ «. {~² «B :º ì (Griffin and Goldberg 1963; Aoki et al. 1974; Hein et al. 1979; Corliss et al. 1982; Aoki and Kohyama 1998). Hein et al.(1979)f Ê{æ Þ~ Ö²ÿ*ö² W" òöB zÖêJb BÒ>æ pº Ò ö "~ Ê{æÞ& 'b Ú J: Ï>B />º Òf ÿï· 7_ öB />º FeOOH& Ö~ ;W>î "Ë~ & . ~æò ôf f zÖêJb~ æî W>º ®C7b jãÒÞf Ò¯¢Þ& Ê.

(7) Paleo-latitude of the Intertropical Convergence Zone in the Northeast Pacific. Fig. 4. Latitudinal variations of smectite and illite in the surface sediments of the cores from this study and Jung et al. (1998). PC 03-03-N11 (N11) was excluded because the surface sediments were not analyzed for the mineral composition.. {æÞf z® º Ò ö V¢ ï· &*ê ö ª~º 'b Ú Ê{æÞ& zÖêJb~ æî ö ~ ;W>îj &ËWj B~& (Griffin and Goldberg 1963; Aoki et al. 1974; Corliss et al. 1982; Aoki and Kohyama 1998). Òæ~ &¦ª òöBº Ê{æÞ~ · Ã& ~º *öB Ò¯¢Þ º 9 ç 7b & VB . 6 PC 02-01-02öBº Ê{æÞ& Ö^æ º 250 cm ~¦öB Ò¯¢Þf þ jãÒ Þ~ · /Ï® Ã&~º ·çj º, º Òæ ~ Ê{æÞ& zÖêJb~ æî" &7 &N ®rj æ . æ~ Ê{æÞ~ Wö J: ÚÊ 'Ëj ~º&ö &Bº ¶ò~ ¦b ï && ®&Ë~ . ~æò, Aoki and Kohyama(1998)& " Ë :f ?, J:~ Ï& Ê{æÞ~ Wö jº Ò¢ ¦ª'b / &ËWj VB >º ì æò Î ò~ ['bö OÖÏ ô ÖÂ>º 6j J r Ê{æÞ~ ·j Ö;~º º²º jö ©b 6B . ß® Aoki and Kohyama(1998) Ê{æÞ ·" Ò¯¢Þ ·"~ ç&&êº Ê{æÞ~ · zÖêJb~ /ö ~B 'Ëj A ®rj æ . V¢B ò~ ['bö B &V>º Ê{æÞ · &*ê .> Ã&~º *çf zÖêJb~ 'Ë &*ê 'böB Ã&~ ®rj æ .. 251. *ê æ~ §ï· ['b 7 <2 µm ~~ òöBº ¢¢Þ · 70% çb Ö Ö^~² ª~ & 20oN¦Vº &*ê .> 6N 6²~, 'ê ÎöBº Ê{æÞ& &Ë Ö^ 7bWj (Griffin and Goldburg 1963; Corliss et al. 1982; Lyle et al. 2002). 7bç~ *êê æzº 'ê> Z&¢ &î ¾æ¾º ³WVö 'b~ Vöæ æ zö V (Lyle et al. 2002). §ï· ÞB³" § ÿZ³ö ~ 7¾ § &öB Vö C'" ¢¢Þ& ³¦ 'b Ö^ >, Îÿï·ö Bº ÎÿZ³~ 'Ëb 7ÁÎ &b¦V Vö zÖêJW bî Ö^~V r^ (Griffin and Goldberg 1963; Lyle et al. 2002). ò~ 7bW æzº B J« ï· 'b 7bW~ *êê æ zf ¾ ¢~~, V¢B &*êöB ¾æ¾º Ê{æ Þ~ Ã& *ç 6 'ê>Z& ¦"öB ¾æ¾º Î> Vö 'b~ / Ã&f ö V zÖêJb~ / Ã&& öb 'B . *Ò ÿï· 'ê> Z&~ *~& 5-10oN Òö *~j J r(Pickard and Emery 1982), "Ëf JKj <º . ® Ö"º 'ê>Z&~ §ã ãê 10oN ¦"ö B ['b Ú Ê{æÞ& ¢¢Þ Ö^æº ·çj «{® " ®b(Fig. 4), 7bª ßWf " 'ê>Z&~ *~ æz¢ C&Úº FÏ ~² Ï > ® . Þ 9oN ÎöB j v "çò~ ['b f ¢¢Þ& Ê{æÞö j Ö^~² ¾æ¾º, º ÒæöB ¢>'b &V>º 7bç *êê æz ·ç" ç>>º Ö"¢ (Fig. 4). * *çö & «{ C *Ò {B ¶òòbº ® &Ë~, *êö V ¢>' æz·ç¢ &ËW" æ ;æzö V æ' *ç¢ &ËW Îv¢ VB > ì . ~æò, .' *êê 7bç~ æz·ç öê ®~, 'ê>Z&~ §¦f Î¦öB &V>º ßû' 7bç~ æz·ç(¢¢Þ ³¦ 'ê>Z& §" Ê{æÞ& ³¦ 'ê>Z& Î~ 'ê 5 Îï·)" 'ê>Z& "¾öB &V>º /Ï 7b ç~ æz·çf Ê{æÞ-¢¢Þ~ ç&' ·~ æz¢ Û~ 'ê>Z&~ " *~¢ º' > ®rj æ .

(8) êê %b`9 æz B "çò~ êê 7bW æzº ç¦öB ¢¢Þ& Ö^~, ê~ Ã&ö V¢ Ê{æÞ~ · 6N Ã&~ ¢; ê ~öBº Ê{æÞ& ¢¢Þ ôjæº ·çj . º ['b.

(9) 252. Hyeong, K. et al.. 7bç~ *êê æz·ç" Ö FÒ~, f ?f p ö V 7bç~ æzº §ï· º¶òöB ê B : ® (Griffin and Goldberg 1963; Leinen and Heath 1981; Aoki and Kohyama 1998; Lyle et al. 2002). Ê{æÞ& Ö^ Ê{æÞ-¢¢Þ *& ~¦ ~ 'b~ 7bWf pö V /Ï æz¢ æ pº (Figs. 2, 3). º 7bç~ >ç' æz& æ ' zÖÿ" ?f V*ö zÖêJb~ / jò, ËV*ö ö n;'b /B zÖêJb~ 'Ëj A~rj æ . ¢ 7bWf Î ï·~ 'b~ "çòöB ßû'b &V> (Griffin and Goldberg 1963), ò~ ¦ 'b '~ã" Vöæö ®ÚB Îï·" Ö FÒ®rj ¾æÞ . ['b~ *êê 7bW æzöB Æ~ :f ?, "çòöB &V>º Ê{æÞ-¢¢Þ * &º 'ê>Z&~ *~f &7 &N ®º ©b C>, B3V ÿn 'ê>Z&~ *~æzö ~B ' Ëj Aº ©b 6B . ¯, 'ê>Z&& B3V ÿn *Ò §ãö *~ ®îb, Ö" ÎÿZ³~ 'Ë *Ò *êræ Ö"B C > ®. . îC~ Vö ¢¢Þf FÒ 6j J r, îC~ pö V 6² ·ç 6 'ê>Z&~ *~ æzf &N ®º ©b CB . &ËWf Vö BB 'ê>Z&~ *~ö & Ö"ö ~ ÝAB . Flohn(1981)f æö Ò~º &ê ~~ ·j .G~, ¢ Û ·" 'êÒ~ NêV¢ 'b êÖ~ Î ~~ · ö êV îJ^ö 'ê>Z&& 12oN ¦"ö *~® º "Ëj BV: ® . 6 Pettke et al.(2002)f ~f §¦ 30o12'N æöB j LL44-GPC3 "çò 'b~ Nd ÿ*ö² æz· ç ¢ Û~ 4,000ò j* 'ê>Z&& 23oN ¦" ö *~®î º Öj êÂ~& . öê Lyle et al. (2002)º æb¦V £ 1,200 km BãöB *êê (7oN-33oN) j "çò~ 7bW æz ¢ Û~ 20 Maö 'ê>Z&& £ 27oNö *~ ®îb , ê ê³ Îê~ *Ò~ *~ö ©b " Ë~& . ÚÚ :f ? º 'ê>Z&& B 3V ÿn *Ò §ãö *~ ®î º ÛB "Ë j BV~ ® . Ê{æÞ-¢¢Þ *&~ pº *êöB &* ê &B 6N »jæº ãËWj (Figs. 2, 3), _ 6 16o12'Nö *~ PC 02-01-02~ ãÖ £ 8 Ma(Hyeong et al. 2003), Ò 8-10oN Òö *~ ò~ ãÖ 2-4 Ma(Lyle et al. 2002; ·>Ö¦ 2004). 6N 0Úæº ãËj . º *ê~ ò& &*ê òö j~ b& 'ê>Z&~ 'Ëj A~r j ~~, V¢B 'ê>Z&& B3V ê 6N Î~ ~ *Ò *~ö %~ º V~ Ö"f ¢~ . ® öB 2kB 7bW~ êê æz·çf §ÿZ³" ÎÿZ³~ ãê¢ º 'ê>Z&~ &ê *~ æz¢ ¾ V~ ®º ©b C&rb , V¢B Ê{æÞ-¢¢Þ *&~ Úê' _ G;j Û~ ;{ êV îJ^ ê~ 'ê> Z&~ &ê *~ º; &Ë ©b 6B .. 6. Ö. . §ÿï· C-CæöB jB "çò~ 7bW f òj æ~ 'ê>Z&ö & ç&' *~f B3V ÿn B 'ê>Z& *~æz~ 'Ëb ¢¢ Þf Ê{æÞ~ · *ê 5 êö V¢ Úê'b æz~º ·çj . ['b Ú ¢¢Þ~ · f 17oNöB 65%b &8j &*ê .> 6²~ 9o30'NöBº ²8 31%¢ ¾æÞ . >& Ê{æÞ~ ·f 17oNöB 11% &Ë Ô, &* ê &B 6N Ã&~ 9o30'NöBº 56%¢ Næ. . f ? &*ê &B 'b Ú Ê{æÞ& 6N Ö^æº ·çf 'ê>Z&ö &ròæB zÖ êJb ³¦ Î> Vö 'b~ / Ã& r ^b CB . ['b Ú Ê{æÞ& ¢¢Þ Ö^æº 10oN ¦"f 'ê>Z&~ §ã ãêf ¢~~, 7bª ßWf " 'ê>Z&~ * ~ æz¢ C&Úº FÏ~² Ï > ® . "ç 'b~ êê 7bW æz¢ ÚÚ Ö" ~ ¦ .> ¢¢Þ& 6²~ Ê{æÞ~ · Ã &~º ãË Â]~² &VB . º B3V ÿn 'ê >Z&& *Ò §ãö *~bB ÎÿZ³~ ' Ë *êræ 'Ëj ~º Ö" CB . 6 Ê {æÞ& Ö^æº ê& *ê .> pÚæº ãËf 'ê>Z&& B3V ê 6N Î~ F © b 6B .. Ò. Ò. º ·>Ö¦& æö~º &7b¶ö BB Òë" ·ö~ Bc~"B(PE896-00)~ æöj Aj >¯>î . >¯ö ôf êæj " &¶ ö^V ö ª" N*Ò^ ßö ªþ 6ÒÒ, ß® ò&jf 7bªCö > '", ^;V þ 6Òãî ..

(10) Paleo-latitude of the Intertropical Convergence Zone in the Northeast Pacific. ^^ò ·>Ö¦. 2003. & 7b¶ö öÒ B(I). ·>Ö ¦ B, CRPM197-00-1582-5. 683 p. ·>Ö¦. 2004. & 7b¶ö öÒ B(I). ·>Ö ¦ B, CRPM197-00-1582-5. 770 p. Aoki, S. and N. Kohyama. 1998. Cenozoic sedimentation and clay mineralogy in the northern part of the Magellan Trough, Central Pacific Basin. Mar. Geol., 148, 21-37. Aoki, S., N. Kohyama, and T. Sudo. 1974. An iron-rich montmorillonite in a sediment core from the north eastern Pacific. Deep-Sea Res., 21, 865-875. Biscaye, P.E. 1965. Mineralogy and sedimentation of recent deep-sea clay in the Atlantic Ocean and adjacent seas and oceans. Geol. Soc. Am. Bull., 76, 803-831. Corliss, B.H. and C.D. Hollister, et al. 1982. A paleoenvironmental model for Cenozoic sedimentation in the central North Pacific. p. 277-304. In: The Ocean Floor. ed. by R.A. Scrutton and M. Talwani. John Wiley & Sons, Chichester. Flohn, H. 1981. A hemispheric circulation asymmetry during late Tertiary. Geol. Rundsch., 70, 725-736. Griffin, J.J. and E.D. Goldberg. 1963. Clay-mineral distribution in the Pacific Ocean. p. 728-741. In: The Sea. Vol. 3. ed. by M.N. Hill. John Wiley & Sons, New York. Halbach, P., G. Friedrich, and U. von Stakelberg. 1988. The manganese nodule belt of the Pacific ocean. Ferdimand Enke, Stuttgart. 254 p. Hein, J.R., H.W. Yeh, and E. Alexander. 1979. Origin of iron-rich montmorillonite from the manganese nodule belt of the north equatorial Pacific. Clays Clay Miner., 27, 185-194. Hovan, S.A. 1995. Late Cenozoic atmospheric circulation intensity and climatic history recorded by eolian deposition in the eastern equatorial Pacific ocean, Leg 138. p. 615-625. In: Proceedings of the Ocean Drilling Program, Scientific Results 139. eds. by N.G Pisias, L.A. Mayer, T.R. anecek, A. Palmer-Julson, and T.H. van Andel. College Station, TX (Ocean Drilling Program). Hyeong, K.S., C.M. Yoo, S.H. Park, J.W. Moon, K.Y. Lee, and K.H. Kim. 2003. Trace and rare earth elemental compositions of the operationally defined eolian dust fraction of core sediments from the northeast equotorial Pacific and their implications on paleolocation of the intertropical convergence zone. Geol. Soc. Am., Abstracts with Program, Vol. 35, No. 6. Johnson, D.A. 1972. Ocean-floor erosion in the equatorial Pacific. Geol. Soc. Am. Bull., 83, 3121-3144.. 253. Jung, H.S., C.B. Lee, K.S. Jeong, and J.K. Kang. 1998. Geochemical and mineralogical characteristics in twocolor core sediments from the Korea Deep Ocean Study (KODOS) area, northeast equatorial Pacific. Mar. Geol., 144, 295-309. Lienen, M. and G.R. Heath. 1981. Sedimentary indicatiors of atmospheric activity in the northern hemishpere during the Cenozoic. Paleogeogr., Paleoclimatol., Paleoecol., 36, 1-21. Lyle, M., P.A. Wilson, T.R. Janecek, et al. 2002. Proceedings of the Ocean Drilling Program, Initial Reports 199: College Station, TX (Ocean Drilling Program). Müller, P.J. and A. Mangaini. 1980. Organic carbon decomposition rates in sediments of the Pacific manganese nodule belt dated by Th-230 and Pa-231. Earth Planet. Sci. Lett., 51, 94-114. Pettke, T., A.N. Halliday, and D.K. Rea. 2002. Cenozoic evolution of Asian climate and sources of Pacific seawater Pb and Nd derived from eolian dust of sediment core LL44-GPC3. Paleoecanography, 17, 3-1-3-13. Pickard, G.L. and W.J. Emery. 1982. Descriptive physical oceanography: an introduction. 4th ed. Pergamon Press. 249 p. Piper, D.Z. and J.R. Blueford. 1982. Distribution, mineralogy, and texture of manganese nodules and their relation to sedimentation at DOMES Site A in the equatorial north Pacific. Deep-Sea Res., 29, 927-952. Piper, D.Z. and M.E. Williamson. 1977. Composition of Pacific ocean ferromanganese nodules. Mar. Geol., 23, 41-55. Pisias, N.G. and A.C. Mix. 1997. Spatial and temporal oceanographic variability of the eastern equatorial Pacific during the late Pleistocene: Evidence from Radiolaria microfossils. Paleoceanography, 12, 381-393. Rea, D.K. 1994. The paleoclimatic record provided by eolian deposition in the deep sea: The geologic history of wind. Rev. Geophys., 32, 159-195. Skornyakova, N.S. and I.O. Murdmaa. 1992. Local variations in disribution and composition of ferromanganese nodules in the Clarrian-Clipperton nodule province. Mar. Geol., 103, 381-405. Shultz, L.G. 1964. Quantitative interpretation of mineralogical composition from X-ray and chemical data for the Pierre shale. Geological Survey Professional Paper 391-C, United States Government Printing Office, Washington. C31p. Received Apr. 14, 2004 Accepted May 25, 2004.

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