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Evidence from Lateral Variation in Stable Isotopes in Paleosols of the Siwalik Group, Northern Pakistan

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Evidence from Lateral Variation in Stable Isotopes in Paleosols of the Siwalik Group, Northern Pakistan The structure and rate of late Miocene expansion of C4 plants: Evidence from lateral variation in stable isotopes in paleosols of the Siwalik Group, northern Pakistan Anna K. Behrensmeyer* Department of Paleobiology, MRC 121, National Museum of Natural History, Smithsonian Institution, P.O. Box 37012, Washington, DC 20013-7012, USA Jay Quade Dept. of Geosciences and the Desert Laboratory, University of Arizona, Tucson, Arizona 85721, USA Thure E. Cerling Dept. of Geology and Geophysics, University of Utah, Salt Lake City, Utah 84112, USA John Kappelman The University of Texas at Austin, Department of Anthropology, University Station C3200, Austin, Texas 78712, USA Imran A. Khan Deputy Director General, Geological Survey of Pakistan, Jauhar Town, Phase–II, Lahore, Pakistan Peter Copeland Department of Geosciences, University of Houston, Houston, Texas 77204, USA Lois Roe 907 Eton Way, Neptune, New Jersey 07753, USA Jason Hicks Denver Museum of Nature and Science, 2001 Colorado Blvd., Denver, Colorado 80205, USA Phoebe Stubblefi eld Forensic Science Department, Babcock Hall, Room 208, University of North Dakota, Grand Forks, North Dakota 58202, USA Brian J. Willis Shallow Marine Stratigraphy, Chevron Energy Technology Company, 1500 Louisiana St., Houston, Texas 77002, USA Claudio Latorre CASEB-Departamento de Ecología, Pontifi ca Universidad Católica de Chile, Santiago 114-D and Institute of Ecology & Biodiversity, Las Palmera 3425, Santiago, Chile ABSTRACT buried soil carbonates in Siwalik Series sedi- channel fi ll, crevasse-splay, and fl oodplain ments exposed in the Rohtas Anticline, north- environments. δ13C results show that near This study uses stable isotope variation central Pakistan. Revised, high-resolution the beginning (8.0 Ma) and after (4.0 Ma) the within individual Mio-Pliocene paleosols to magnetostratigraphy and a new 40Ar/39Ar period of major ecological change, vegetation investigate subkilometer-scale phytogeog- date provide improved age control for the was homogeneously C3 or C4, respectively, raphy of late Miocene vegetation change in 2020 m Rohtas section. Carbon isotope regardless of paleo-landscape position. In the southeast Asia between ca. 8.1 and 5 Ma, a results capture lateral variability of C3 ver- intervening period, there is a wide range of time interval that coincides with dramatic sus C4 plants at fi ve stratigraphic levels, R11 values overall, with C4 grasses fi rst invading global vegetation change. We examine trends (8.0 Ma), R15 (6.74–6.78 Ma), R23 (5.78 Ma), the drier portions of the system (fl oodplain through time in the distribution of low-lati- R29 (4.8–4.9 Ma), and upper boundary tuff surfaces) and C3 plants persisting in moister tude grasses (C4 plants) and forest (C3 plants) (UBT; 2.4 Ma), using detailed sampling of settings, such as topographically lower chan- on Indo-Gangetic fl oodplains using carbon paleosols traceable laterally over hundreds of nel swales. Although abrupt on a geologic δ13 δ18 ( C) and oxygen isotopic ( O) values in meters. Paleosols and the contained isotopic timescale, changes in abundance of C4 plants results can be assigned to three different dep- are modest (~2% per 100,000 yr) compared *E-mail: [email protected]. ositional contexts within the fl uvial sediments: to rates of vegetation turnover in response to Expansion of C4 plants in Miocene of Pakistan glacial and interglacial climate changes in the can be traced laterally over hundreds of meters. with previous age information based on mag- Quaternary. Earlier research documented a These paleosols formed on the aggrading fl ood- netostratigraphy and radiometric dating of sharply defi ned C3 to C4 transition in Paki- plains of large rivers and record vegetation several volcanic ashes that occur in its upper stan between 8.1 and 5.0 Ma, based on verti- patterns on a portion of the vast sub-Himala- part (Opdyke et al., 1979; 1982; GSA Data cal sampling, but this higher-resolution study yan piedmont alluvial plain at a paleolatitude Repository item part one1). In this paper, we reveals a more gradual transition between of ~29–31°N (Opdyke et al., 1979; Tauxe and report new magnetostratigraphic results and an 40 39 8.0 and 4.5 Ma in which C3 and C4 plants Opdyke, 1982). Macroplant remains and pol- Ar/ Ar date for the Rohtas section that allow occupied different subenvironments of the len are poorly preserved in the Pakistan Siwalik more secure correlations to the geomagnetic Siwalik alluvial plain. Group, and pedogenic carbon isotope values are reversal time scale (GRTS) and provide better δ18O values as well as δ13C values of soil an important proxy for characteristics of Mio- calibration of the timing and rate of the Siwalik carbonate increase up section at Rohtas, sim- cene-Pleistocene paleovegetation. C3-C4 transition and the age of paleosol carbon- ilar to isotope trends in other paleosol records Stable isotopic evidence from paleosol car- ates used in this and previous studies. from the region. Spatially, however, there is bonate, groundwater cements, and fossil teeth δ13 δ18 no correlation between C and O values shows that C4 vegetation underwent a dramatic GEOLOGIC SETTING at most stratigraphic levels. This implies that expansion in the late Miocene (Stern et al., the changes in soil hydrology brought about 1994; Quade and Cerling, 1995; Cerling et al., The Siwalik Group occurs continuously from by the shift from forest to grassland (i.e., an 1997, 2003; Morgan et al., 1994; Quade and Afghanistan and western Pakistan to Burma increase in average soil evaporation) did not Roe, 1999; Levin et al., 2004; Nelson, 2007). and consists of fl uvial sediments deposited in produce the shift through time in δ18O val- The timing of this expansion appears to be dia- the foreland basin formed by the collision of ues. We interpret the trend toward heavier chronous globally, occurring fi rst at low lati- the Indian subcontinent with Asia over the past soil carbonate δ18O values as a response to tudes and later at higher latitudes (Cerling et al., 18 Ma. Miocene strata are faulted and folded changes in external climatic factors such as a 1997). By the Plio-Pleistocene, the expansion adjacent to and south of the overthrust belt, net decrease in rainfall over the past 9 Ma. was complete in many low-latitude areas. Most resulting in widespread exposures of sedimen- C4 plants are grasses, so this expansion marks tary rocks, which are rich in vertebrate fos- Keywords: carbon isotopes, oxygen isotopes, the emergence of tropical and temperate lati- sils. The Siwalik Group in Pakistan consists of paleosol, Miocene, Pakistan. tude grasslands at the expense of C3 vegetation fi ve formations (Kamlial, Chinji, Nagri, Dhok (woody plants as well as C3 grasses), which in Pathan, and Soan), amounting to a total thick- INTRODUCTION many places was probably woodland and forest ness of >4 km in the Potwar-Kohat depression in (Quade et al., 1995; Hoorn et al., 2000). Palyno- Pakistan (Tauxe and Opdyke, 1982; Johnson et Stable isotopes preserved in ancient soils logical study of the Siwalik sequence in Nepal al., 1985). In the Potwar area, the chronostratig- are being used to track vegetation and climate shows little evidence of grass prior to 7.0 Ma raphy is based on paleomagnetism, supple- changes through time within many different (Hoorn et al., 2000). Based on previous research mented by isotopic dating of rare volcanic ash Cenozoic rock sequences (Quade and Cerling, in Pakistan, the Siwalik C3-C4 transition began beds (Johnson et al., 1982a, 1982b, 1985). The 1995; Cerling et al., 1997; Latorre et al., 1997; between 7.8–8.1 Ma and was complete (i.e., formations are characterized by different propor- Kleinert and Strecker, 2001; Fox and Koch, 2004; most δ13C values >−2‰) by ca. 5 Ma. tions of sand versus mudstone, refl ecting shifts Levin et al., 2004; Wynn, 2004). These stable We specifi cally address the following ques- through time in the geographic position of large- isotope records typically are based on vertical tions in this paper: (1) what is the lateral vari- to small-scale rivers and their alluvial deposits as sampling through long stratigraphic sequences, ability in pedogenic carbon and oxygen values well as changes in foreland basin subsidence and and each sample is assumed to represent average in Siwalik paleosols and how does this change sediment input (Burbank and Beck, 1991; Willis, δ13C and δ18O values for that time interval. Lat- through time; (2) how does isotopic variability 1993a, 1993b; Khan et al., 1986, 1997; Zaleha, eral variations in δ13C and δ18O at a given point within single paleosols relate to topographic and 1997). Studies of the fl uvial sedimentology of the in time have seldom been documented but could geologic features of the fl oodplain environments; Miocene through Pleistocene deposits document provide information on vegetation complex- (3) what do these results indicate with regard to the changing infl uence of mountain (Himalaya)- ity that contributes to more detailed ecological rates and patterns of vegetation change during sourced (“blue-gray”) versus lowland-sourced reconstructions of evolving paleo-landscapes the overall C3-C4 transition in northern Pakistan; (“buff”) rivers (Raynolds, 1981; Behrensmeyer (Sikes 1994; Levin et al., 2004). and (4) what are the implications of these iso- and Tauxe 1982; Burbank and Beck, 1991; Barry A major shift from C3 to C4 vegetation tope trends for understanding the dynamics of et al., 2002). These studies provide specifi c infor- between ca. 8.0 and 5.0 Ma was previously doc- this fl uvial paleo-ecosystem in particular and mation on fl ow directions and velocities, channel umented in the Siwalik Series of northern Paki- environmental change in general? size and geometry, and fl oodplain aggradation. stan (Quade and Cerling, 1995; Cerling et al., To address these questions we studied Siwa- Paleochannel belts in the Jhelum area were on 1997; Quade and Roe, 1999).
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