Estadios Isotópicos Marinos. Estratigrafía de los isótopos del oxígeno
DOI:
https://doi.org/10.17735/cyg.v36i3-4.94172Palabras clave:
Períodos glaciares-interglaciares; Pleistoceno; cronología; paleoclimaResumen
La estratigrafía de los isótopos del oxígeno no es un método de datación por sí mismo, sino que es necesaria la comparación de nuestros registros con secuencias isotópicas “globales “para su correlación. La proporción de los isótopos del oxígeno (O16, O18) en compuestos moleculares que contienen este elemento (p.ej. H2O, CaCO3) varía en función de la temperatura. La relación O18/O16 (δO18) nos ayuda no solo a determinar las temperaturas en el pasado geológico de la Tierra, sino también a identificar los cambios en el volumen de hielo en casquetes polares, promovidos por las variaciones en los parámetros orbitales (precesión, oblicuidad, excentricidad). La sucesión de épocas glaciares e interglaciares a lo largo del Cuaternario ha quedado registrada en sondeos oceánicos profundos (CaCO3 de los caparazones de organismos bentónicos y planctónicos) definiéndose estadios isotópicos mediante números pares (glaciares) e impares (interglaciares). La escala isotópica ha adquirido un valor cronoestratigráfico al construirse modelos de edad a partir de dataciones isotópicas (C14, series de Uranio, para los estadios isotópicos más recientes), la escala paleomagnética, y, sobre todo, mediante su ajuste astronómico. La correlación de nuestros registros con las secuencias isotópicas así establecidas nos permite establecer su cronología e interpretar la respuesta paleoclimática en nuestras latitudes ante las variaciones paleoclimáticas globales.
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