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Oceanic processes of upper ocean heat content associated with two types of ENSO

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Abstract

The spatiotemporal variability of equatorial Pacific upper ocean heat content (HC) and subsurface heat during two types of El Niño-Southern Oscillation (ENSO), namely eastern and central Pacific (EP and CP) types, is investigated using subsurface ocean heat budget analysis. Results show that HC tendencies during both types of ENSO are mainly controlled by oceanic heat advection beneath the mixed layer to the thermocline, and the role of net surface heat flux can be neglected. The most important three terms are the zonal and vertical advections of anomalous heat by climatological currents (QU 0 T′, QW 0 T′) and zonal advection of climatological heat by anomalous current (QU′T 0). The large contribution of QU 0 T′ extends from west to east along the equatorial Pacific. The considerable contribution of QU′T 0 is confined to the east of 160°W, and that of the QW 0 T′ is observed in the central Pacific between 180°E and 120°W. In particular, a major contribution of QW 0 T′ is also observed in the far eastern Pacific east of 100°W during EP ENSO. There is also a small contribution from meridional advection of climatological heat by anomalous current (QV′T 0). In contrast, the meridional advection of anomalous heat by climatological currents (QV 0 T′) and vertical advection of climatological heat by anomalous current (QW′T 0) are two damping factors in the HC tendency, with the former dominating. Differences in spatial distribution of the heat advection associated with the two types of ENSO are also presented. We define a warm water heat index (WWH) as integrated heat content above 26 kg m−3 potential density (26σ ɵ ) isopycnal depth within 130°E–80°W and 5°S–5°N. Further examination suggests that the recharge–discharge of WWH is involved in both types of El Niño, though with some differences. First, it takes about 42 (55) months for the evolution of a recharge–discharge cycle during an EP (CP) ENSO. Second, the EP El Niño event peaks during the discharge phase, 7–8 months after the recharge time. The CP El Niño peaks during the recharge phase, 4–5 months before the recharge time. The locations of HC anomalies in the El Niño mature phase relative to those at recharged time explain why the EP and CP El Niño peak in different stages of the recharge–discharge process.

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Acknowledgements

We thank two anonymous reviewers for their constructive and valuable suggestions. This work was supported by the Natural Science Foundation of China (NSFC) (Nos. 41476017, 41330963, 41506023), NSFC-Shandong Joint Fund for Marine Science Research Centers (No. U1406401), Fund for Innovative Research Groups of the NSFC (No. 41421005), and the “Strategic Priority Research Program” of the Chinese Academy of Sciences (No. XDA01010101).

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Authors and Affiliations

  1. Institute of Oceanology, Chinese Academy of Sciences, Nanhai Rd. No. 7, Qingdao, 266071, China

    Junqiao Feng, Dunxin Hu & Shoude Guan

  2. Key Laboratory of Ocean Circulation and Waves, Chinese Academy of Sciences, Qingdao, China

    Junqiao Feng, Dunxin Hu & Shoude Guan

  3. Laboratory for Ocean and Climate Dynamics, Qingdao National Laboratory for Marine Science and Technology, Qingdao, China

    Junqiao Feng, Dunxin Hu & Shoude Guan

  4. Department of Atmospheric Sciences, SOEST, University of Hawai’i at Mānoa, Honolulu, HI, USA

    Junqiao Feng, Fei-fei Jin & Shoude Guan

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  1. Junqiao Feng
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Correspondence to Junqiao Feng.

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Feng, J., Jin, Ff., Hu, D. et al. Oceanic processes of upper ocean heat content associated with two types of ENSO. J Oceanogr 74, 219–238 (2018). https://doi.org/10.1007/s10872-017-0452-y

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