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The natural gamma radiation (NGR) data were acquired each 10 cm (see details below) on fluvio-lacustrine and palustrine sediment materials, from the continental CDB1 drill-core located in the Rennes Basin (Chartres de Bretagne, France, geographic coordinates: 48.04412074N; 1.71899076W, Elevation: +37m NGF, Nivellement Général de France). The studied geological time interval covers the Eocene-Oligocene transition interval, roughly from 31 to 38.5 Ma. NGR measurements were conducted by the Semm Logging company during the drilling campaign of the CINERGY project (CDB1 borehole) during summer 2010, under the supervision of BRGM (Bureau de Recherches Géologiques et Minières, France), on behalf the contracting authority of Chartres-de Bretagne. The main objective of the CINERGY project was to explore the Cenozoic cover of the Armorican shield preserved in a small strike-slip basin. The CINERGY Project was funded by the BRGM, the AELB (Agence de l'Eau Loire-Bretagne) and the ADEME (Agence de l'Environnement et de la Maitrise de l'Energie) French agencies. The NGR probe used during the CDB1 well logging consists of a scintillation detector (sodium iodide crystal coupled to a photo-multiplication tube), which converts gamma rays into electric pulses. The measured values are expressed in API (American Petroleum Institute) unit. This unit was calculated using a linear interpolation of raw data expressed in pulses per second (pps) according to a calibration set with a very stable source, the radioactivity of which is known in API unit. Because disintegration is a random phenomenon, raw measurements taken every 2 cm are integrated over a 25 cm long window and restored at a 10 cm step, which is consistent both with the crystal size and the average dip of the strata, nearly 15 degrees.

The physical properties of sea ice, including salinity, sea ice temperature, and sea ice texture as well as isotopic composition (oxygen and hydrogen) were analyzed from samples collected on the CAATEX 2019 expedition to the central Arctic Ocean (between North Pole and Svalbard) in late summer 2019. In addition, isotope samples were collected from precipitation, melt ponds, and under-ice seawater. Data was collected to understand the formation mechanisms of sea ice in the area. Ice cores were collected with an ice corer, and measurements (temperature) were directly carried out from ice cores after retrieval. From an additional ice core, samples (salinity and isotopes) were collected and melted onboard. Salinity of samples was measured onboard using a conductivity probe, while samples for isotopic composition were placed in sample bottles and measured at the FARLAB (University of Bergen) after the expedition . A complete ice core was brought back for texture analysis of the sea ice and processed at the freezer lab at the Norwegian Polar Institute. Texture was examined by first slicing ice samples very thin by use of a microtome. These thin ice slices were observed in polarized light that reveals the crystal structure of the ice. This data includes the photographs taken of the ice cores in natural light and in polarized light.

The physical properties of sea ice, including salinity, sea ice temperature, and sea ice texture as well as isotopic composition (oxygen and hydrogen) were analyzed from samples collected on the CAATEX 2019 expedition to the central Arctic Ocean (between North Pole and Svalbard) in late summer 2019. In addition, isotope samples were collected from precipitation, melt ponds, and under-ice seawater. Data was collected to understand the formation mechanisms of sea ice in the area. Ice cores were collected with an ice corer, and measurements (temperature) were directly carried out from ice cores after retrieval. From an additional ice core, samples (salinity and isotopes) were collected and melted onboard. Salinity of samples was measured onboard using a conductivity probe, while samples for isotopic composition were placed in sample bottles and measured at the FARLAB (University of Bergen) after the expedition . A complete ice core was brought back for texture analysis of the sea ice and processed at the freezer lab at the Norwegian Polar Institute. Texture was examined by first slicing ice samples very thin by use of a microtome. These thin ice slices were observed in polarized light that reveals the crystal structure of the ice. This data includes the photographs taken of the ice cores in natural light and in polarized light.

The Knapps Narrows core was drilled at 38.72129N, -76.33162W on the Eastern Shore of Maryland. The cored target interval lies between 84-102 meters in the Nanjemoy Formation. Calcareous nannofossil biozonation was established in conjunction with paleomagnetic data, allowing us to date the interval to approximately 53.7 mya. Benthic foraminiferal and bulk carbon isotope data allowed for further refinement of the dating of this interval, allowing us to identify ETM2 and H2 on the basis of carbon isotope stratigraphy. For analyses of benthic foraminifera 4-6 Anomalinoides acutus specimens were picked from the 180-250 μm size fraction at each interval. Dinoflagellate cyst assemblages were counted in order to allow for paleo-environmental analysis. Benthic foraminiferal δ18O and TEX86 temperature proxies were compiled over the interval of interest. Semi-quantitative clay mineral assemblages were used to test for changes in the weathering response over hyperthermal intervals. There is excellent agreement between the δ18O and TEX86 temperature proxies, although the highest temperatures do not correspond to either hyperthermal event. There is a noticeable increase in illite content during the ETM2 interval, and an absence of kaolinite. Dinoflagellate assemblages suggest changes in marine paleo-environmental conditions were driven by long-term trends rather than immediate responses to the hyperthermal events.

The physical properties of sea ice, including salinity, sea ice temperature, and sea ice texture as well as isotopic composition (oxygen and hydrogen) were analyzed from samples collected on the CAATEX 2019 expedition to the central Arctic Ocean (between North Pole and Svalbard) in late summer 2019. In addition, isotope samples were collected from precipitation, melt ponds, and under-ice seawater. Data was collected to understand the formation mechanisms of sea ice in the area. Ice cores were collected with an ice corer, and measurements (temperature) were directly carried out from ice cores after retrieval. From an additional ice core, samples (salinity and isotopes) were collected and melted onboard. Salinity of samples was measured onboard using a conductivity probe, while samples for isotopic composition were placed in sample bottles and measured at the FARLAB (University of Bergen) after the expedition . A complete ice core was brought back for texture analysis of the sea ice and processed at the freezer lab at the Norwegian Polar Institute. Texture was examined by first slicing ice samples very thin by use of a microtome. These thin ice slices were observed in polarized light that reveals the crystal structure of the ice. This data includes the photographs taken of the ice cores in natural light and in polarized light.

The physical properties of sea ice, including salinity, sea ice temperature, and sea ice texture as well as isotopic composition (oxygen and hydrogen) were analyzed from samples collected on the CAATEX 2019 expedition to the central Arctic Ocean (between North Pole and Svalbard) in late summer 2019. In addition, isotope samples were collected from precipitation, melt ponds, and under-ice seawater. Data was collected to understand the formation mechanisms of sea ice in the area. Ice cores were collected with an ice corer, and measurements (temperature) were directly carried out from ice cores after retrieval. From an additional ice core, samples (salinity and isotopes) were collected and melted onboard. Salinity of samples was measured onboard using a conductivity probe, while samples for isotopic composition were placed in sample bottles and measured at the FARLAB (University of Bergen) after the expedition . A complete ice core was brought back for texture analysis of the sea ice and processed at the freezer lab at the Norwegian Polar Institute. Texture was examined by first slicing ice samples very thin by use of a microtome. These thin ice slices were observed in polarized light that reveals the crystal structure of the ice. This data includes the photographs taken of the ice cores in natural light and in polarized light.

The antipatharian coral Antipathella wollastoni is commonly found in the Macaronesia (Cape Verde, Madeira, Canaries and the Azores Archipelago). In the Azores Archipelago the species forms dense populations and coral gardens on island slopes between 15-520 m water depth. Here, we present data from two experiments on the embryo and larval survival of A. wollastoni under two different seawater temperatures (21°C and 23­°C). Embryos were collected after spawning of mother colonies in aquaria. In the first experiment, we monitored the number of embryos for 24 h after spawning, while in the second experiment we monitored the number of embryos and planulae (larvae) for a total of 35 h.

We present an age model for the 651 m deep Skytrain Ice Rise ice core (79°44.5'S, 78°32.7'W). The top 2000 years have previously been dated using age markers interpolated through annual layer counting. Below this, we align the Skytrain core to the AICC2012 age model using tie points in the ice and air phase, and apply the Paleochrono program to obtain the best fit to the tie points and glaciological constraints. In the gas phase, ties are made using methane and, in critical sections, δ18Oair; in the ice phase ties are through 10Be across the Laschamps Event, and through ice chemistry related to long-range dust transport and deposition. This strategy provides a good outcome to about 108 ka (~605 m). Beyond that there are signs of flow disturbance, with a section of ice probably repeated. Nonetheless values of CH4 and δ18Oair confirm that part of the last interglacial (LIG), from about 117-126 ka (617-628 m), is present and in chronological order. Below this there are clear signs of stratigraphic disturbance, with rapid oscillation of values in both the ice and gas phase at the base of the LIG section. Based on methane values, the warmest part of the LIG and the coldest part of the penultimate glacial are missing from our record. Ice below 631 m appears to be of age >150 ka.