d18O (CO04MGNG01A): interpretation1_variable: 'temperature and salinity' has been replaced by 'temperature'
d18O (CO04MGNG01A): interpretation2_seasonality: 'annual' has been replaced by 'Annual'
d18O (CO04MGNG01A): interpretation2_variable: 'd18O_seawater' has been replaced by 'seawaterIsotope'
d18O (CO04MGNG01A): interpretation3_variable: 'T_water' has been replaced by 'temperature'

d18O (CO04MGNG01A): paleoData_longName: '' has been replaced by 'AD'
depth (MATc79ceefe7c): paleoData_longName: '' has been replaced by 'AD'
year (MATfd9cf377f1): paleoData_units: 'AD' has been replaced by 'yr AD'
year (MATfd9cf377f1): paleoData_longName: '' has been replaced by 'AD'

McGregor, H. V. and Gagan, M. K.: Western Pacific coral δ18O records of anomalous Holocene variability in the El Nino-Southern Oscillation, Geophysical Research Letters, 31(11), n/a–n/a, doi:10.1029/2004gl019972, 2004.

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.

automated carbonate preparation device (Kiel device) + Finnigan Mat 252 mass spectrometer

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

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,

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).