Abstract
In this study we attempted to assess whether seasonal upwelling or a steady thermocline persisted at the western margin of the Tethys Ocean during the late Turonian–early Coniacian interval. For this scope, we employed novel and published stable oxygen isotope (δ18O) data of various organisms (bivalves, bivalves, brachiopods, fish and belemnites). New seasonally resolved temperature estimates were based on the δ18O record of sequentially sampled inoceramid (Inoceramus sp.) and rudist (Hippurites resectus) shells from the Scaglia Rossa and Gosau deposits of northern Italy and western Austria, respectively. Diagenetic screening was performed using reflected light, cathodoluminescence (CL), scanning electron microscopy (SEM) and stable isotope analysis. Originally preserved δ13C and δ18O values were used to characterize the lifestyle of the bivalves and detect vital effects that could have biased oxygen isotope-based temperature reconstructions. Inoceramid δ18O values provide–for the first time–information on temperatures of Tethyan benthic waters, which were, on average, 14.4 ± 0.6 °C and fluctuated seasonally within a range of less than 2 °C. Such a thermal regime is in line with the temperatures postulated for late Turonian boreal water masses and support the existence of a cold water supply from the North Atlantic to the Tethyan bottom. Bottom cooling, however, did not affect the shallow water environment. In fact, the rudist-based temperature estimates for shallow water environment revealed a mean annual range of 11 °C, between 24 and 35 °C (assuming a seasonally constant δ18Ow = 1.0 ‰), which are among the warmest temperatures recorded over the entire Late Cretaceous. Our findings, thus, suggest a strong thermal and food web decoupling between the two environments. The absence of a seasonal vertical homogenization of different water bodies suggests the existence of a steady thermocline and, therefore, contrasts with the presence of an active coastal upwelling in the region as hypothesized by previous authors.
Highlights
Following the Aptian-early Turonian ‘supergreenhouse’ event (90–95 Ma) [1,2], the Late Cretaceous world experienced a time interval of significant global cooling [3,4,5]
Numerical climate simulations indicate that deep water production in the North Atlantic was possible during most of the Late Cretaceous [8,9,10], and geochemical proxy data suggest that migration of cold, high latitude water masses into the equatorial Atlantic Ocean and Central Europe occurred as early as the middle and late Turonian [11,12,13]
Under the CL, the outer shell layer (OSL) was non-luminescent, and scanning electron microscopy (SEM) imaging revealed the preservation of the original fibrous calcitic ultrastructure of the shell
Summary
Following the Aptian-early Turonian ‘supergreenhouse’ event (90–95 Ma) [1,2], the Late Cretaceous world experienced a time interval of significant global cooling [3,4,5]. Numerical climate simulations indicate that deep water production in the North Atlantic was possible during most of the Late Cretaceous [8,9,10], and geochemical proxy data suggest that migration of cold, high latitude water masses into the equatorial Atlantic Ocean and Central Europe occurred as early as the middle and late Turonian [11,12,13] During this interval, North Atlantic waters flooded the northwestern Tethys Basin [14] increasing the dissolved oxygen levels at the bottom of the ocean [15,16,17], which drove to the formation of the reddish-pinkish shale, marls and limestones of the Scaglia Rossa Formation [18,19,20]. It is possible that oceanic cooling did not pervade the shallowest habitats at the northwestern margin of the Tethys and thermal decoupling (instead of upwelling) existed between the bottom and the shallow water environments during the late Turonian–early Coniacian
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