Textural and Geochemical Characteristics of Ferromanganese Crusts from the Lomilik and Litakpooki Seamounts, Marshall Islands, West Pacific

서태평양 마샬제도 Lomilik와 Litakpooki 해저산 망간각의 조직 및 지화학적 특성

  • Woo, Kyeong-Sik (Department of Geology, Kangwon National University) ;
  • Park, Sung-Hyun (Deep-sea Resources Research Center, Korea Ocean Research and Development Institute) ;
  • Jung, Hoi-Soo (Deep-sea Resources Research Center, Korea Ocean Research and Development Institute) ;
  • Moon, Jai-Yoon (Deep-sea Resources Research Center, Korea Ocean Research and Development Institute) ;
  • Lee, Kyeong-Yong (Deep-sea Resources Research Center, Korea Ocean Research and Development Institute) ;
  • Choi, Youn-Ji (Deep-sea Resources Research Center, Korea Ocean Research and Development Institute)
  • 우경식 (강원대학교 지구과학부) ;
  • 박숭현 (한국해양연구소 심해저자원연구센타) ;
  • 정회수 (한국해양연구소 심해저자원연구센타) ;
  • 문재운 (한국해양연구소 심해저자원연구센타) ;
  • 이경용 (한국해양연구소 심해저자원연구센타) ;
  • 최윤지 (한국해양연구소 심해저자원연구센타)
  • Published : 2001.02.28


Six ferromanganese crusts from the Lomilik and Litatfooki seamounts in the Marshall Islands were analyzed for texture, geochemistry and stratigraphy to delineate the paleoceanographic conditions. The crusts can be divided into three layers; 1) outermost massive layer (Layer 1), 2) middle porous Fe-oxides rich layer infllled with biointemal clasts (Layer 2), and 3) innermost massive layer cemented and/or replaced by carbonate fluoapatite (CFA) (Layer 3). The Layer 1 contains higher Mn, Co, Ni, and Mg than other two layers, and the Layer 2 was relatively more enriched in Fe, Al, Ti, Ba, Cu, and Zn. However, the Layer 3 shows higher Ca and P and lower Mn, Fe, Co, and Ni contents than overlying two layers. Based on the Co-chronometry, the crusts are postulated to have begun to grow from 56-31 Ma (early Eocene to Oligocene). The boundaries between layers 1 and 2, and layers 2 and 3 are dated to be 7-3 Ma and 26-14 Ma, respectively. High contents of Ca and P in Layer 3 clearly indicate that the layer had been phosphatized prior to the formation of Layer 2. Considering the well-preserved mjcrostructures in Layer 3, it is unlike that the crusts themselves were recrystallized in suboxic condition. Also, the lower Co concentrations in Layer 3 may imply that the Co supply was not constant during the formation of Layer 3. Layer 2, characterized by the porous texture, grew over Layer 3 during 26-9 Ma. Internal biogenic sediments including foraminifera within the original cavities and the enrichment of organophillic elements such as Ba, Cu, and Zn, suggest that Layer 2 have below high production regions. Also, high content of allumino silicate components may indicate increased terrigeneous input during the formation of Layer 2. The Layer 2. The Layer 1 has been subjected to little diagenetic influence since the Pliocene.



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