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Fig. 7 in Mollusc biodiversity in late Holocene nearshore environments of the Caspian Sea: A baseline for the current biodiversity crisis

Fig. 7. Late Holocene Novocaspian gastropod species from Turali, with indication of sample and collection number. A Clathrocaspia gmelinii: M0203, RGM.1309848 B Clessiniola variabilis: M0204, RGM.1309864 C Ecrobia grimmi: M0202, RGM.1309863 D Laevicaspia sieversii: M0204, RGM.1309849 E Laevicaspia kolesnikoviana: M0221, RGM.1309850 F Laevicaspia conus: M0204, RGM.1309851 G Turricaspia spica: M0202, RGM.1309858 H Turricaspia sp. indet. M0222, RGM.962401. I Abeskunus brusinianus: low morph, M0204, RGM.962355 J Abeskunus brusinianus: high morph, M0204, RGM.962355 K Theodoxus pallasi: M0204, RGM.130985, L. Theodoxus pallasi: M0220, RGM.1309862, M Abeskunus exiguus, M0204, RGM.962357. Scale bars 1 mm.

Fig. 6 in Mollusc biodiversity in late Holocene nearshore environments of the Caspian Sea: A baseline for the current biodiversity crisis

Fig. 6. Late Holocene Novocaspian bivalve species from Turali, with indication of sample and collection number. LV displayed on the left, RV on the right. A–B Adacna laeviuscula (Eichwald, 1829). A M0222, RGM.962359 B M0222, RGM.962358 C–D Adacna vitrea (Eichwald, 1829) C M0221, RGM.962360 D M0221, RGM.962361 E–F Hypanis plicata (Eichwald, 1829) E M0221, RGM.962362 F M0221, RGM.962363 G–H Monodacna albida (Logvinenko & Starobogatov, 1967) G M0202, RGM.962364 H M0202, RGM.962365 I–J Monodacna caspia (Eichwald, 1829) I M0204, RGM.962367 J M0205, RGM.962368 K–L Monodacna semipellucida (Logvinenko & Starobogatov, 1967) K M0222, RGM.962369 L M0222, RGM.962370 M–N Dreissena caspia (Eichwald, 1855) M M0222, RGM.962371 N M0202, RGM.962372 O–P Dreissena elata (Andrusov, 1897) O M0203, RGM.962375 P M0221, RGM.962376 Q–R Dreissena grimmi (Andrusov, 1890) Q M0203, RGM.962374 R M0202, RGM.962373. Scale bars 5 mm.

Fig. 2 in Mollusc biodiversity in late Holocene nearshore environments of the Caspian Sea: A baseline for the current biodiversity crisis

Fig. 2. Schematic representation of sections Turali 1-3. Asterisks (*) denote calibrated 14C ages BP. Small case letters refer to sedimentary units: a. eastwards-dipping bay fill, b. eastwards-dipping bay fill, c. sand with shells along eastward-dipping foresets, d. deformed laminated silts and sands, e. massive gravel beds, f. coarsegrained pebble lag, g. slightly dipping sand layers with shells, h. low-angle clinoforms with pebbles and shells, i. stratified silt stone, lagoonal, j. silt layer with shells, k. Aeolian interval, l. stratified silt stone, lagoonal.

Fig. 3 in Mollusc biodiversity in late Holocene nearshore environments of the Caspian Sea: A baseline for the current biodiversity crisis

Fig. 3. Paired Didacna eichwaldi (Turali-2, sample M0205) exposed just below the water table of the Great Turali Lake. Width of the shells approximately 2 cm. Photograph SBK, 2002.

Fig. 8 in Mollusc biodiversity in late Holocene nearshore environments of the Caspian Sea: A baseline for the current biodiversity crisis

Fig. 8. Reconstruction of Turali Bay, c. 2300 calyr BP. The palaeocoastline is approximatly based on the estimated lake level reconstructed for the time of deposition.

Fig. 5 in Mollusc biodiversity in late Holocene nearshore environments of the Caspian Sea: A baseline for the current biodiversity crisis

Fig. 5. Late Holocene Novocaspian bivalve species from Turali, with indication of sample and collection number. LV displayed on the left, RV on the right. A–B Cerastoderma sp. A [non C. rhomboides (Lamarck, 1819)] A M0215, RGM.961896 B M0215, RGM.962391 C–D Cerastoderma glaucum (Bruguière, 1789) C M0216, RGM.962390 D M0216, RGM.962389 E–F Didacna baeri (Grimm, 1877) E M0204, RGM.962379 F M0204, RGM.962380 G–H Didacna eichwaldi (Krynicki, 1837) G M02-05, RGM.961900 H M02-05, RGM.961900 I–J Didacna parallela (Bogachev, 1932) I M0202, RGM.962383 J M0202, RGM.962384 K–L Didacna protracta (Eichwald, 1841) K M0202, RGM.962386 L M0222, RGM.962385 M–N Didacna pyramidata (Grimm, 1877) M M0202, RGM.962387 N M0222, RGM.962388 O–P Didacna trigonoides (Pallas, 1771) O M0215, RGM.962378 P M0215, RGM.962377. Q–R Didacna barbotdemarnii (Grimm, 1877) Q M0222, RGM.962420 R M0221, RGM.962421. Scale bars 5 mm.

Fig. 9 in Mollusc biodiversity in late Holocene nearshore environments of the Caspian Sea: A baseline for the current biodiversity crisis

Fig. 9. Box core residue (sample M0267, c. 2 km off shore Turali at a water depth of 9.4 m) separated into the dark Novocaspian (left) and light 20th Century (right) fractions defined in the text. Largest shell c 1.5 cm across.

Fig. 4 in Mollusc biodiversity in late Holocene nearshore environments of the Caspian Sea: A baseline for the current biodiversity crisis

Fig. 4. Rarefaction curves of the Turali samples with 95% confidence interval and extrapolated species richness for double sample size.

Fig. 1 in Mollusc biodiversity in late Holocene nearshore environments of the Caspian Sea: A baseline for the current biodiversity crisis

Fig. 1. Geographic context of study site. (a) Map of the Caspian Sea. Source bathymetry: Kostianoy et al. (2005): Fig. 1 (p. 7). (b) Location of the outcrops treated in this paper. Tu1-Tu5 represent outcrops Turali 1-5. Brown ridges are Holocene Novocaspian beach barriers (see Kroonenberg et al., 2007). (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.)

opencc-zeroAug 2019View details →

Data from: Resilience of lake biogeochemistry to boreal-forest wildfires during the late Holocene

Novel fire regimes are expected in many boreal regions, and it is unclear how biogeochemical cycles will respond. We leverage fire and vegetation records from a highly flammable ecoregion in Alaska and present new lake-sediment analyses to examine biogeochemical responses to fire over the past 5300 years. No significant difference exists in δ13C, %C, %N, C:N, or magnetic susceptibility between pre-fire, post-fire, and fire samples. However, δ15N is related to the timing relative to fire (Χ2=19.73, p<0.0001), with higher values for fire-decade samples (3.2±0.3‰) than pre-fire (2.4±0.2‰) and post-fire (2.2±0.1‰) samples. Sediment δ15N increased gradually from 1.8±0.6‰ to 3.2±0.2‰ over the late Holocene, probably as a result of terrestrial-ecosystem development. Elevated δ15N in fire decades likely reflects enhanced terrestrial nitrification and/or deeper permafrost-thaw depths immediately following fire. Similar δ15N values before and after fire decades suggest that N cycling in this lowland-boreal watershed was resilient to fire disturbance. However, this resilience may diminish as boreal ecosystems approach climate-driven thresholds of vegetation structure, permafrost thaw, and fire.

opencc-byJun 2022View details →

Bison jaw (late Holocene). Big Bone Lick, KY

Late Holocene Bison mandible (Bison bison) from 1971 excavations at Big Bone Lick, Boone Co., KY. The bulging jaw below the molars is a pathology suggesting infection at the time of death. Scanned in June 2022 at Big Bone Lick, State Park (#1971.2.2). Source: Objaverse 1.0 / Sketchfab

opencc-by-4.0Jan 2022View details →

FIGURE 2 in A vanished ecosystem: Sophora microphylla (Kōwhai) dominated forest recorded in mid-late Holocene rock shelters in Central Otago, New Zealand

FIGURE 2. The Kawarau Region, showing shelter locations (red dots) along the Kawarau River.

opencc-by-4.0Jul 2024View details →

Mid-Late Holocene coral calcification dynamics: Deciphering climatic and environmental effects

Over the past four decades, a marked decrease in coral calcification has occurred across the world's tropical reefs, closely linked to climate change and human-activity impacts. However, how natural and human-induced factors influence coral calcification remains unclear due to limited understanding of the geological past. This study addresses this gap by investigating the calcification parameters of 82 Porites corals from the northern South China Sea, with growth periods covering distinct climatic epochs during the Mid-Late Holocene, including the Holocene Climate Optimum, 4.2 ka BP event, Medieval Climate Anomaly, Little Ice Age, and Current Warm Period. Our findings show a gradual increase in coral skeletal density towards the present, and varied linear extension and calcification rates between warm and cold phases and between pre- and post-industrial periods. This suggests that temperature plays a pivotal role in controlling coral calcification, with contingent influences from volcanic activity and solar radiation. Notably, the linear extension and calcification rates were significantly reduced during the Current Warm Period, suggesting a surpassing impact of contemporary human activities over the natural variability on coral calcification. This raises concerns about the future prospects of coral reefs in the face of ongoing climate change and increasing human-activity impacts.

opencc-by-4.0Jan 2022View details →

Data for Klaes et al. High-resolution stalagmite stratigraphy supports the Late Holocene tephrochronology of southernmost Patagonia. Comms. Earth Environ. (2022)..

This data set comprises the LA-ICP-MS, ICP-MS, EPMA and NanoSIMS measurements as well as SEM imagery presented in the research paper 'High-resolution stalagmite stratigraphy supports the Late Holocene tephrochronology of southernmost Patagonia' by Klaes et al. The Th-U data of the revised chronology of stalagmite MA1 with the calculated correction values according to Budsky et al. (2016) are also included. In addition, stable isotope data from Schimpf et al. (2011) with the revised version of the age-depth model are given. For detailed information on the analyses (e.g., instruments used), the user is kindly referred to the methods section of the article.

opencc-by-4.0Sep 2022View details →

Variability of the East Asian winter monsoon since mid-late Holocene

Wind speed of the East Asian winter monsoon since 4.4 ka was quantitatively reconstructed at a high temporal resolution (~4 years) based on grain size of a core sediment from a well preserved mud patch in the North Yellow Sea.

opencc-zeroMay 2023View details →

~550-year climate periodicity in the Yunnan-Guizhou plateau during the late mid-Holocene: Insights and implications

This is the Supporting Information for Li et al. "550-Year Climate Periodicity in the Yunnan-Guizhou Plateau during the late Mid-Holocene: Insights and Implications" published in Geophysical Research Letters. The data comes from a stalagmite in southwestern China (27° 4' N, 105° 5' E). The dataset includes the speleothem 230Th dating data (Table S1 in Supporting Information S1), the speleothem 230Th dating, 13C, lamina thickness, 18O, Sr/Ca and Mg/Ca data (Table S2), the updated 14C database from archaeological sites in southwestern China (Table S3), the calculated minimal occupation events as the unit of analysis by combining more than one 14C date (Table S4) and the summed 14C probability (SCP) records (Table S5). The Supporting Information S1 includes a pdf file (available through Zenodo) provided also contains details on the methods of all the lab work, the results of the trace elements, the demonstration of annual lamina and application of least-squares fit, the practices of calculating summed 14C probability (SCP) distributions in southwestern China and a discussion on how ENSO and local precipitation can influence the proxies. Additionally, there are supporting figures (Figure S1-S8) for the main text in Supporting Information S1. The speleothem 230Th dating, 13C, lamina thickness, 18O, Sr/Ca and Mg/Ca data in this study are also available in the public paleoclimate database of the National Oceanic and Atmospheric Administration (NOAA) (https://www.ncei.noaa.gov/access/paleo-search/study/38059).

opencc-zeroSep 2023View details →

Marine diatoms record Late Holocene regime shifts in the Pikialasorsuaq ecosystem

The Pikialasorsuaq (North Water polynya) is an area of local and global cultural and ecological significance. However, over the last decades, the region has been subject to rapid warming and, in some recent years, the seasonal ice arch that has historically defined the polynya's northern boundary has failed to form. Both factors are deemed to alter the polynya's ecosystem functioning. To understand how climate-induced changes to the Pikialasorsuaq impact the basis of the marine food web, we explored diatom community-level responses to changing conditions, from a sediment core spanning the last 3800 years. Four metrics were used: total diatom concentrations, taxonomic composition, mean size, and diversity. Generalized additive model statistics highlight significant changes at ca. 2400, 2050, 1550, 1200, and 130 cal years BP, all coeval with known transitions between colder and warmer intervals of the Late Holocene, and regime shifts in the Pikialasorsuaq. Notably, a weaker/contracted polynya during the Roman Warm Period and Medieval Climate Anomaly caused the diatom community to reorganize via shifts in species composition, with the presence of larger taxa but lower diversity, and significantly reduced export production. This study underlines the high sensitivity of primary producers to changes in the polynya dynamics and illustrates that the strong pulse of early-spring cryopelagic diatoms that makes the Pikialasorsuaq exceptionally productive may be jeopardized by rapid warming and associated Nares Strait ice arch destabilization. Future alterations to the phenology of primary producers may disproportionately impact higher trophic levels and keystone species in this region, with implications for Indigenous Peoples and global diversity.

publicAug 2019View details →

Data from: Resilience of lake biogeochemistry to boreal-forest wildfires during the late Holocene

Open the record for dataset details and reuse information.

publicDec 2023View details →

~550-year climate periodicity in the Yunnan-Guizhou plateau during the late mid-Holocene: Insights and implications

Open the record for dataset details and reuse information.