『Abstract
　Silicon isotopes in dissolved silicic acid were measured in the upper four kilometers between 4゜N and 3゜S latitude at 110゜W longitude in the eastern Equatorial Pacific. Silicon isotopes became progressively heavier with silicic acid depletion of surface water as expected from biological fractionation. The value of ε estimated by applying a steady-state isotope fractionation model to data from all stations between 4゜N and 3゜S was -0.77±0.12‰ (std. err.). When the analysis was restricted to those stations whose temperature and salinity profiles indicated that they were directly influenced by upwelling of the Equatorial Undercurrent (EUC), the resulting value of ε was -1.08±0.27‰ (std. err.) similar to the value established in culture studies (-1.1‰). When the non steady state Rayleigh model was applied to the same restricted data set the resulting value of ε was significantly more positive, -0.61±0.16‰ (std. err.). To the extent that the equatorial system approximates a steady state these results support a value of -1.1‰ for the fractionation factor for isotopes of Si in the sea. Without the assumption of steady state the value of ε can only be constrained to be between -0.6 and -1.1‰. Silicic acid in Equatorial Pacific Deep Water below 2000 m had a near constant δ³⁰Si of +1.32±0.05‰. That value is significantly more positive than obtained for North Pacific Deep Water at similar depths at stations to the northwest of our study area (0.9-1.0‰) and it is slightly less positive than new measures of the δ³⁰Si of silicic acid from the silicic acid plume centered over the Cascadia basin in the Northeast Pacific (Si(OH)4＞180μM, δ³⁰Si = +1.46±0.12‰ (SD, n=4). We show that the data from the equator and Cascadia basin fit a general trend of increasing δ³⁰Si(OH)4 with increasing silicic acid concentration in the deep sea, but that the isotope values from the Northeast Pacific are anomalously light. The observed level of variation in the silicon isotope composition of deep waters from this single ocean basin is considerably larger than that predicted by current models based on fractionation during opal formation with no isotope effect during dissolution. Confirmation of such high variability in deep water δ³⁰Si(OH)4 within individual ocean basins will require reassessment of the mechanisms controlling the distribution of isotopes of silicon in the sea.』

1. Introduction
2. Material and methods
3. Results and discussion
　3.1. Water masses
　3.2. δ³⁰Si distribution
　　3.2.1. Surface waters
　　3.2.2. Intermediate and deep waters
　3.3. Estimate of the fractionation factor, ε
　　3.3.1. Steady state model
　　3.3.2. Rayleigh model
　　3.3.3. Mixing effects on field estimates of ε
4. Conclusions
Acknowledgments
References