Observation of temperature and velocity from a surface buoy moored in the Shikoku Basin (OMLET-88) —An oceanic response to a Typhoon

Taira, Keisuke; Kitagawa, Sho; Otobe, Hirotaka; Asai, Tomio

doi:10.1007/bf02234956

Cited by 20 publications

(4 citation statements)

References 7 publications

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“…The upper ocean cooling is important because it can suppress the development of TCs [Bender et al, 1993;Wada and Chan, 2008;Lin et al, 2013], including subsequent TCs that cross these cold wakes. The cooling typically ranges from 1 to 6°C [Hazelworth, 1968;Price, 1981;Taira et al, 1993;Cione and Uhlhorn, 2003;Lin et al, 2003;Price et al, 2008]. The sea surface cooling left behind the tropical cyclone can extend hundreds of kilometers adjacent to the storm track in the horizontal direction; vertically, the cooling depth is usually slightly thicker than the prestorm mixed-layer depth [Large et al, 1986].…”

Section: Introductionmentioning

confidence: 99%

Observed three‐dimensional structure of ocean cooling induced by Pacific tropical cyclones

Wang

Johnson

et al. 2016

Geophysical Research Letters

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Sea surface cooling along tropical cyclone (TC) tracks has been well observed, but a complete understanding of the full three‐dimensional structure of upper ocean TC‐induced cooling is still needed. In this study, observed ocean temperature profiles derived from Argo floats and TC statistics from 1996 to 2012 are used to determine the three‐dimensional structure of TC‐induced cooling over the northwest Pacific. The average TC‐induced sea surface temperature change derived from Argo reaches −1.4°C, which agrees well with satellite‐derived estimates. The Argo profiles further reveal that this cooling can extend to a depth of ~30 m and can persist for about 20 days. The time scale of cooling recovery is somewhat longer in subsurface layers between a depth of ~10–15 m. Over the ocean domain where the mixed layer is shallower (deeper), the cooling is stronger (weaker), shallower (deeper), and more (less) persistent. The effect of initial MLD on the cooling derived from Argo observations may be only half of the idealized piecewise continuous model of tropical cyclone. These findings have implications for the total upper ocean heat content change induced by northwest Pacific TCs.

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Section: Introductionmentioning

confidence: 99%

Observed three‐dimensional structure of ocean cooling induced by Pacific tropical cyclones

Wang

Johnson

et al. 2016

Geophysical Research Letters

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“…The figure on the title page shows a water temperature of 18°C during the EUE event on October 11, 2021, at Station 2 (see Figure 1c for Station 2 location). Even during extreme cold weather events such as tropical cyclones, the surface water temperature decreases only by 1°-8°C (e.g., Taira et al, 1993;Cione and Uhlhorn, 2003;Vecchi and Soden, 2007;Lin et al, 2013;E. Lee et al, 2016;Li et al, 2020).…”

Section: Introductionmentioning

confidence: 99%

Extreme Upwelling Events in the Seas of the Alor Kecil, Alor Island, Indonesia

Wirasatriya¹,

Susanto²,

Setiawan³

et al. 2023

Oceanog

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Upwelling is a process by which deep, colder, higher-nutrient waters are brought to the sea surface. In the tropics, an indicator that an upwelling event has occurred is lowering of sea surface temperatures (SSTs) to 25°–27°C from a mean of ~28°C. Based on more than one year of in situ data, we observed an unusual extreme upwelling event (EUE) when the near-surface temperature (NST) dropped by 10°C within one hour during the spring tide in Mulut Kumbang Strait of Alor Kecil. The extreme minimum NST during this EUE was ~12°C, and the upward displacement speed of the cold water was ~0.012 m s–1. The increase in salinity from ~30‰ to 34‰–36 ‰ during the decrease in NST indicates a deep source for the cold water mass . From bathymetry and CTD data, the source of the cold water mass was a deep basin (>300 m) located at the southern part of Pantar Strait. In this basin, the temperature at 270 m depth can be as low as 8°C. We suggest that tidal sloshing (i.e., the back-and-forth movement of water) brings the cold water mass through a channel that connects this deep basin to Mulut Kumbang Strait. Interactions between semi-diurnal (M2, S2, and N2) tidal components strongly modulate the tidal signal with a period of nearly one month. That EUEs only occur from August to November also suggests a strong monsoonal influence. Because tides are predictable, we suggest that future EUEs are predictable.

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“…The maximum SST cooling generally occurs to the right of the TC track in the northern hemisphere [15,[20][21][22], although it can be observed to the left of the TC track [23,24] or exactly along the track [25]. The magnitude of SST cooling induced by the passage of TCs has been reported to range from 1 • C to 10 • C [14,[26][27][28][29]. Dare and McBride [30], using a compositing approach, studied the response of SST to the passage of TCs in the global ocean and found that the maximum cooling occurs~1 day after TC passage and mean maximum SST cooling is about −0.9 • C.…”

Section: Introductionmentioning

confidence: 99%

Recovery of Tropical Cyclone Induced SST Cooling Observed by Satellite in the Northwestern Pacific Ocean

et al. 2021

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Based on the satellite observed sea surface temperature (SST), the recovery of SST cooling induced by the tropical cyclones (TCs) over the northwestern Pacific Ocean is investigated. The results show that the passage of a TC induces a mean maximum cooling in the SST of roughly −1.25 °C. It was also found that most of this cooling (~87%) is typically erased within 30 days of TC passage. This recovery time depends upon the degree of cooling, with stronger (weaker) SST cooling corresponding to longer (shorter) recovery time. Further analyses show that the mixed layer depth (MLD) and the upper layer thermocline temperature gradient (UTTG) also play an important role in the SST response to TCs. The maximum cooling increases ~0.1 °C for every 7 m decrease in the MLD or every 0.04 °C/m increase in the UTTG. The combined effects of MLD and TC intensity and translation speed on the SST response are also discussed.

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Observation of temperature and velocity from a surface buoy moored in the Shikoku Basin (OMLET-88) —An oceanic response to a Typhoon

Cited by 20 publications

References 7 publications

Observed three‐dimensional structure of ocean cooling induced by Pacific tropical cyclones

Observed three‐dimensional structure of ocean cooling induced by Pacific tropical cyclones

Extreme Upwelling Events in the Seas of the Alor Kecil, Alor Island, Indonesia

Recovery of Tropical Cyclone Induced SST Cooling Observed by Satellite in the Northwestern Pacific Ocean

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