JpGU-AGU Joint Meeting 2017

Presentation information

[EE] Poster

B (Biogeosciences) » B-PT Paleontology

[B-PT03] [EE] Biomineralization and the Geochemistry of Proxies -Field ecology, Laboratory culture and Paleo

Sat. May 20, 2017 10:45 AM - 12:15 PM Poster Hall (International Exhibition Hall HALL7)

convener:Takashi Toyofuku(Japan Agency for Marine-Earth Science and Technology (JAMSTEC)), Hiroshi Kitazato(University Reform Office, Tokyo University of Marine Science and Technology (TUMSAT)), Jelle Bijma(Alfred-Wegener-Institut Helmholtz-Zentrum f?r Polar- und Meeresforschung)

[BPT03-P09] Temporal size change of the middle Miocene planktonic foraminiferal species Paragloborotalia siakensis (LeRoy)

*Suzuki Takuma1, Hiroki Hayashi1, Osamu Sasaki2 (1.Interdisciplinary Graduate School of Science and Engineering, Shimane University , 2.Tohoku University Museum)

Keywords:planktonic foraminifera, temporal size distribution, global correlation , Miocene, IODP

The extinction of Miocene planktonic foraminiferal species Paragloborotalia siakensis (LeRoy) defines the uppermost boundary of planktonic foraminiferal Zone N.14 (Blow, 1969). Many workers have examined the taxonomy of the morphospecies, however it has still been controversy. Bolli and Saunders (1982) proposed that Globorotalia siakensis (= P. siakensis of this study) should be a junior synonym for Groborotalia mayeri Cushman. The geologic time scale of Berggren et al. (1995) is also based on this taxonomic criterion, and the extinction of “Neogloboquadrina mayeri” was used for his zonal boundary. Zachariasse and Sudijono (2012) conducted morphological analyses using a scanning electron microscope (SEM) for P. siakensis collected near the type locality. They also examined holotypes of both species and concluded that P. siakensis could be distinguished from G. mayeri by its suture and surface structure. Okada and Hayashi (2013) carried out taxonomical examinations for P. siakensis obtained from IODP Site U1338 in the eastern equatorial Pacific, which is located in the central part of the distribution area. Through their SEM analysis, most specimens could be correlated with the holotype of P. siakensis with few exceptions. In addition, their diagrams of morphological analyses indicate that holotypes of P. siakensis and G. mayeri should be contained within the same morphological space of the specimens from Site U1338. They also reported the size distribution pattern of P. saikensis from approximately 15 to 11 Ma and pointed out that the size distribution pattern would have a good potential for global correlation and needs more study. The purpose of this study is to refine the temporal size distribution of P. siakensis and to establish global correlation based on the size distribution pattern of the species.
We conducted size measuring of this species at Site U1338 from approximately 16 to 11 Ma. At the same time, we performed X-ray microcomputed tomography (XMCT) analyses and thin section observations at selected horizons. Seventy-five samples at an interval of approximately 0.05 Ma from the site were used for this study. These samples had been already examined for planktonic foraminiferal assemblage (Hayashi et al. 2012). Then, total 6895 specimens of P. siakensis were measured in maximum diameter. The size distribution was discussed with respect to previous geochemical and paleontological data. In the next step, we are examining the size distribution at the Site U1337 near the Site U1338. And some three-dimensional images of specimens collected from characteristic horizons were acquired by XMCT. The CT images enable us to visualize the inner structure such as the form of chambers, ontogenetic growth pattern, and density distribution in each test. Based on CT images, we can estimate the three-dimensional morphologic comparison, degree of maturation and obesity of each test. For mineralogical approaches, thin sections of foraminiferal tests were observed by a polarization microscope.
In a result, we detected twice giantisms and twice dwarfings in the size distribution pattern. The cycle of size change was approximately 2 Ma. One of the dwarfing events could be correlated with Mi3 event (Miller et al., 1991). Therefore, this dwarfing event could be caused by cooling of sea surface water. According to 3D profiles of foraminiferal chambers, tests of relatively small specimens were composed of both high and low CT value layers. In contrast, the larger tests were generally composed of a pair of low CT value layers. Considering previous CT studies, we assume that the difference in the inner layers might reflect the growth the rate for each individual: pair of low CT value layers might mean relatively rapid growth rate.