rank: NA

scope: climate

rank: NA

scope: climate

rank: NA

scope: climate

rank: NA

scope: climate

rank: NA

scope: climate

rank: NA

scope: climate

rank: NA

scope: climate

rank: NA

scope: climate

basis: We find strong correlations between coral y18O, precipitation, and OLR, but also between coral y18O and SST

direction: decrease/increase

interpDirection: decrease/increase

scope: climate

variable: temperature

variableDetail: sea surface

variableGroup: temperature and salinity

scope: climate

scope: climate

basis: Core piM correlates more strongly with precipitation and OLR than COI-5 (Table 1). Note that years of high rainfall coincide with years of large negative coral y18O anomalies in the wet season (and high amplitudes of the annual cycle,

direction: positive

inferredMaterial: seawater

integrationTime: 2

integrationTimeBasis: A simple chronology based on these density bands in both corals temporally aligned anomalous 18O-depleted years precisely in the same years (e.g., 1972?1973, 1982? 1983). During these years, there were noted positive precipitation and/or SST anomalies. We then assigned February 15 to the most negative isotopic values. This is, on average, the wettest month. We then interpolated linearly between the anchor points to obtain bimonthly records of coral y18O.

integrationTimeUnits: month

mathematicalRelation: linear

rank: 1

scope: isotope

seasonality: subannual

variable: seawaterIsotope

variableGroup: EffectiveMoisture

variableGroupDirection: negative

variableGroupOriginal: d18O_seawater

coefficient: NA

fraction: NA

basis: However, over the entire time interval compared, maximum variations of mean summer SST are 1jC, which would account for approximately 0.20x in coral y18O (Juillet- Leclerc and Schmidt, 2001). Over the same period, mean summer coral y18O varies by as much as 0.7x (piM) and 0.4x (COI-5) (Fig. 4); i.e., the maximum SST contribution to the coral isotopic signal is 29% (piM) and 50% (COI-5).

direction: negative

inferredMaterial: seawater

integrationTime: 2

integrationTimeBasis: A simple chronology based on these density bands in both corals temporally aligned anomalous 18O-depleted years precisely in the same years (e.g., 1972?1973, 1982? 1983). During these years, there were noted positive precipitation and/or SST anomalies. We then assigned February 15 to the most negative isotopic values. This is, on average, the wettest month. We then interpolated linearly between the anchor points to obtain bimonthly records of coral y18O.

integrationTimeUnits: month

mathematicalRelation: linear

rank: 2

scope: isotope

variable: temperature

variableGroup: Temperature

variableGroupDirection: negative

variableGroupOriginal: T_water

coefficient: NA

fraction: NA

scope: isotope

coefficient: NA

fraction: NA

rank: NA

basis: We find strong correlations between coral y18O, precipitation, and OLR, but also between coral y18O and SST

interpDirection: decrease/increase

scope: climate

variable: temperature

variableDetail: sea surface

variableGroup: temperature and salinity

scope: climate

scope: climate

basis: However, over the entire time interval compared, maximum variations of mean summer SST are 1jC, which would account for approximately 0.20x in coral y18O (Juillet- Leclerc and Schmidt, 2001). Over the same period, mean summer coral y18O varies by as much as 0.7x (piM) and 0.4x (COI-5) (Fig. 4); i.e., the maximum SST contribution to the coral isotopic signal is 29% (piM) and 50% (COI-5)

direction: decrease

mathematicalRelation: linear

rank: 2

scope: isotope

coefficient: NA

fraction: NA

basis: Core GIM correlates more strongly with precipitation and OLR than COI-5 (Table 1). Note that years of high rainfall coincide with years of large negative coral y18O anomalies in the wet season (and high amplitudes of the annual cycle,

direction: increase

mathematicalRelation: linear

rank: 1

scope: isotope

coefficient: NA

fraction: NA

scope: isotope

coefficient: NA

fraction: NA

rank: NA