Moraines in the Austrian Alps Record Repeated Phases of Glacier Stabilization through the Late Glacial and the Early Holocene

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Braumann, Joerg M. Schaefer, Stephanie Neuhuber, Markus Fiebig This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-1321188/v1 This work is licensed under a CC BY 4.0 License Status: Published Journal Publication published 12 Jun, 2022 Read the published version in Scientific Reports → Version 1 posted 8 You are reading this latest preprint version Abstract Climate is currently warming due to anthropogenic impact on the Earth’s atmosphere. To better understand the processes and feedbacks within the climate system that underlie this accelerating warming trend, it is useful to examine past periods of abrupt climate change that were driven by natural forcings. Glaciers provide an excellent natural laboratory for reconstructing the climate of the past as they respond sensitively to climate oscillations. Therefore, we study glacier systems and their behavior during the transition from colder to warmer climate episodes, focusing on the period between 15 and 10 ka. Using a combination of geomorphological mapping and beryllium-10 surface exposure dating, we reconstruct ice extents in two glaciated valleys of the Silvretta Massif in the Austrian Alps and find that the general ice retreat during the deglaciation after the Last Glacial Maximum (LGM) was interrupted by glacier stabilization during the Oldest Dryas to Bølling transition (moraine age: 14.4 ± 1.0 ka), during the Younger Dryas (YD; 12.9-11.7 ka), and during the Early Holocene (EH; 12–10 ka). The first moraine age group indicates a lateral stable ice margin that postdates the ‘Gschnitz’ stadial (ca. 17–16 ka) and predates the YD. It shows that local inner-alpine glaciers were larger than during the subsequent YD until the onset of the Bølling warm phase (ca. 14.6 ka), or possibly even into the Bølling. The second age group ca. 80 m below the (pre-)Bølling moraine indicates ice extents during the YD cold phase and captures the spatial and temporal fine structure of glacier retreat during this period. The ice surface lowered by 50–60 m through the YD, which is indicative of milder climate conditions at the end of the YD compared to its beginning. Finally, the third age group falls into a period of more substantial warming, the YD–EH transition, and shows discontinuous warming during the glacial to interglacial transition. The new geochronologies synthesized with pre-existing moraine records from the Silvretta Massif evidence three cold phases that punctuated the general post-LGM warming trend, and illustrate the sensitive response of Silvretta glaciers to abrupt climate oscillations in the past. Figures Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 1 Introduction Mountain glaciers are highly sensitive to climate variations, most importantly to changes in summer temperatures and to a lesser extent to changes in precipitation 1 , 2 . This sensitivity is evident in the accelerating deglaciation of alpine regions caused by rapid warming due to increasing greenhouse gas emissions in recent decades 3 , chapter 3 , section 3 . 3 . Deglaciation affects mountain regions in various ways, including altering the hydrological regime in these areas and downstream, impacting ecosystems, and increasing the frequency of natural hazards 4 . Improving our understanding of interactions between the climate system and the cryosphere in the past helps to project the magnitude and impact of environmental change in the future. Glaciers and their shaping of many parts of the earth’s surface in the past 5 , 6 enable us to explore the climate system and how it operates with and without anthropogenic impact. Detailed geomorphological mapping and direct dating of former ice margins allow us to reconstruct glaciers across time and space and to draw conclusions about the climate conditions that drove glacier advance or retreat in the past. Here, we present ice-margin reconstructions of two glaciated valleys in the Austrian Alps, at Jamtal and Fimbatal, covering the Late Glacial (LG) and the Early Holocene (EH) – a period when the climate was transitioning from a glacial to an interglacial mode. LG moraines in the European Alps, especially those deposited during the Younger Dryas (YD, ca. 12.9–11.7 ka) termed ‘Egesen’ moraines, are subject to numerous geochronological studies that provide valuable insights into this last phase of prolonged cooling before Holocene warming 7 . Other periods of climate transition before and after the YD remain more controversial in terms of glacier extents and ice dynamics, for instance, the Bølling-Allerød period (B-A, ca. 14.6–12.9 ka) and the EH (ca. 11.7–9 ka). Although glaciers were presumably much more extensive at the beginning of the B-A compared to the beginning of the EH, they were driven by a similar climatic pattern during both periods: a steep temperature increase which led to rapid deglaciation. For the period between ca. 12 and 10 ka, moraine chronologies from different places in the Alps, including data presented in this study, have shown that ice retreat and therefore warming was not linear, but was interrupted by centennial-scale cooling 8 – 11 . For the (pre-)Bølling period, it is still unclear whether ice retreat was steady and of such magnitude that most glaciers in the European Alps retreated to the highest cirques or disappeared altogether 7 . The objective of this study is to contribute to these less resolved periods and to view climate transitions from glacial to interglacial conditions through the lens of glacial geomorphology. Therefore, we mapped moraine sequences at two alpine valleys, the Jamtal and the Fimbatal, and applied 10 Be surface exposure dating to selected landforms to produce direct spatial and temporal information of former ice extents in the Silvretta Massif. The Silvretta Massif is in the westernmost part of the Eastern European Alps (Figure 1 a). The mountain range belongs to the Upper Eastern Alpine (“Oberostalpin”) tectonic unit and consists of crystalline rocks that have undergone several metamorphic events since their formation during the Precambrian 12 . Lithologies in the valleys include amphibolites, different types of metasediments, and gneisses 13 . Glaciers in the region are temperate and are sensitive to climate oscillations (Figure 2 ). Over the past 150 years, rapidly increasing greenhouse gas emissions and resulting warming have led to the melting of glacial ice across the planet. In the Silvretta region, the ice-covered area has decreased to 32 ± 2 % of the extent of the Little Ice Age (LIA; ca. 1250–1850 CE) in the reference years 2017/2018 (Figure 1 b) 14 . Jamtal glacier – the main ice body at Jamtal – has retreated to a position ca. 2 km upstream from the LIA maximum. In 2018, it covered approximately 2.8 km² with its terminus at an altitude of ca. 2410 m a.s.l. Glaciers at Fimbatal have largely disappeared today with only a few small patches of dead ice left in the uppermost sections of the valley (Figure 1 b). In deglaciated sections of both valleys, sequences of lateral and terminal moraines are preserved that evidence stable ice margins of the past and promise insights into periods when climate conditions were favorable for larger glaciers (Figures 3 - 5 , Figure S2 ). 2 Results A total of 15 rock samples were collected from moraines at Jamtal (n=9) and Fimbatal (n=6). Ages are stratigraphically in order and are presented from old to young, beginning with the Jamtal (JAM) record, followed by the Fimbatal (FMB) record. 10 Be analytical data and boulder ages are presented in Table 1 and in Figures 3 - 5 as well as in the supplement ( Tables S1 and S2, section S4 ). Table 1 10 Be analytical data and corresponding exposure ages of Jamtal samples. Samples were analyzed at the CAMS-LLNL. All samples were measured against the 07KNSTD3110 standard with a ratio of 2.85 x 10 −12 82 . One to two procedural blanks were processed with each batch of samples with ratios ranging from 2.3 to 8.4 x 10 −16 (Table S2). The 10 Be background contaminations measured in the blanks were subtracted from the samples. Exposure ages were calculated with the calculator formerly known as CRONUS-Earth online calculator v3; 83 , using the Swiss 10 Be production rate 84 and choosing the ‘Lm’ scaling scheme. Ages are calculated relative to the sampling year denoted by the first number in the sample ID and are rounded to the nearest 10 years. Uncertainties of boulder ages include the 1σ analytical error and a 1% uncertainty on the carrier concentration. Sample ID Latitude [DD] Longitude [DD] Elevation [m a.s.l.] Av. thickness [cm] Shielding factor Quartz mass [g] 9 Be carrier [g] 10 Be/ 9 Be ratio ±1σ analytical unc. (10 −14 ) 10 Be atoms ±1σ analytical unc. [atoms] 10 Be conc. ±1σ analytical unc. [atoms/g qtz] 10 Be exposure age ±1σ analytical unc. and carrier unc. [yrs] F5b FMB-18-05 46.9436 10.2698 2040 2.1 0.9677 4.5939 0.1821 10.26 ± 0.20 (2.0%) 1283934 ± 25261 278524 ± 5480 14000 ± 280 FMB-19-12 46.9435 10.2699 2041 1.7 0.9702 10.6165 0.1789 19.79 ± 0.37 (1.9%) 2440545 ± 45594 229294 ± 4284 11590 ± 220 F5a FMB-18-04 46.9429 10.2697 2044 1.8 0.9709 42.9287 0.1789 79.07 ± 1.68 (2.1%) 9716105 ± 205863 226122 ± 4791 11460 ± 240 FMB-18-08 46.9438 10.2688 2043 2.0 0.9675 25.5955 0.1787 48.96 ± 0.91 (1.9%) 6008892 ± 111455 234413 ± 4348 11920 ± 220 FMB-18-09 46.9438 10.2689 2042 2.1 0.9703 23.8501 0.1790 34.29 ± 0.64 (1.9%) 4215324 ± 79209 176366 ± 3314 9100 ± 170 FMB-19-13 46.9432 10.2694 2044 1.6 0.9728 10.5569 0.1758 18.60 ± 0.35 (1.9%) 2254712 ± 42127 212986 ± 3979 10760 ± 200 J7 JAM-18-11 46.8904 10.1871 2520 1.3 0.9634 9.2555 0.1806 30.46 ± 0.56 (1.9%) 3778652 ± 70081 407782 ± 7563 14710 ± 270 JAM-19-19 46.8904 10.1875 2522 2.0 0.9607 10.6142 0.1798 34.00 ± 0.64 (1.9%) 4214518 ± 78808 396476 ± 7414 14420 ± 270 JAM-20-23 46.8904 10.1872 2521 2.9 0.9620 11.3598 0.1807 35.08 ± 0.71 (2.0%) 4383259 ± 88749 385607 ± 7807 14130 ± 290 J6 JAM-18-13 46.8901 10.1838 2432 3.4 0.9781 16.5606 0.1806 44.59 ± 0.83 (1.9%) 5532868 ± 103026 333831 ± 6216 12880 ± 240 JAM-19-20 46.8893 10.1865 2445 1.5 0.9604 10.6338 0.1801 26.96 ± 0.50 (1.9%) 3347499 ± 62609 314211 ± 5877 12120 ± 230 J5 JAM-20-24 46.8895 10.1829 2380 2.4 0.9779 6.8428 0.1805 15.93 ± 0.30 (1.9%) 1987961 ± 37023 290103 ± 5403 11620 ± 220 JAM-20-25 46.8893 10.1835 2389 1.7 0.9768 10.9885 0.1798 26.46 ± 0.52 (2.0%) 3289758 ± 64839 299123 ± 5896 11830 ± 230 J3-4 JAM-20-26 46.8898 10.1740 2065 1.8 0.9412 11.5032 0.1796 18.81 ± 0.40 (2.1%) 2335435 ± 49824 202777 ± 4326 10490 ± 220 JAM-20-27 46.8908 10.1733 2047 1.4 0.9499 11.5197 0.1803 20.97 ± 0.39 (1.9%) 2613912 ± 48590 226661 ± 4213 11650 ± 220 At Jamtal , our focus was on a steep (>30°) valley flank that features a right-lateral moraine set which was shaped by a former tributary glacier (Futschöl glacier; Figures 3 a-b, S2, and S3). The uppermost landform selected for 10 Be surface exposure dating is J7 at an elevation of ca. 2520 m a.s.l. (Figure 4 a). The three sampled boulders rest on a till-covered lineament and yield a landform age of 14.4 ± 1.0 ka (Figure S1a) . Around 80 m lower, at ca. 2440 m a.s.l., a sharp-crested moraine ( J6 ) was deposited that consists mainly of fine sediments (Figure 4 b) and features two boulders that qualified for sampling. Corresponding ages are 12.9 ± 0.2 ka and 12.1 ± 0.2 ka. The ice margin geomorphology another level below denoted as J5 (Figure 4 d), differs from J6 in the absence of a distinct ridge and in the abundance of boulders of which two were selected for dating and yield ages of 11.6 ± 0.2 ka and 11.8 ± 0.2 ka. Two boulders in the main valley embedded in lateral and in terminal moraines ( J3–4 , Figure 3 c-d) give ages of 10.4 ± 0.2 ka and 11.6 ± 0.2 ka and extend the Holocene moraine chronology published for the valley by Braumann, et al. 9 . At Fimbatal , samples were collected from two adjacent latero-frontal moraine ridges ( F5a and F5b ) deposited at an elevation of ca. 2040 m a.s.l. (Figure 5 ). The outer ridge ( F5b ) consists of mostly fine sediments and is overgrown by vegetation. It is preserved only on the east side of the creek and has few boulders exposed, two of which were sampled and yield ages of 14.0 ± 0.3 ka (FMB-18-05) and 11.6 ± 0.2 ka (FMB-19-12). Although FMB-18-05 agrees within errors with boulder ages along J7 at Jamtal, we reject the age as an outlier due to its stratigraphic position. A terminal moraine at Fimbatal, which is equivalent to the lateral ice-margin position at Jamtal, should be positioned further downstream. FMB-18-05 probably overestimates the age of F5b, most likely due to inheritance from one or multiple earlier exposure events. The inner ridge ( F5a ) is preserved on both sides of the creek and exhibits a blocky structure in its frontal section caused by the outwash of fine-grained material. Exposure ages of the four boulders along F5a range between 11.9 ± 0.2 ka and 9.1 ± 0.2 ka. The age of FMB-18-09 (9.1 ± 0.2 ka) falls within a period during the Holocene when most glaciers had probably retreated inboard the subsequent LIA ice margin 15 – 17 . For reference, the LIA terminal moraine in this valley is located at an elevation of ca. 2520 m a.sl., i.e. around 500 m higher and almost 7 km upstream of F5a/b (Figure 1 b). These vertical and lateral distances cannot be reconciled with the age and location of FMB-18-09. Therefore, we discard the age for our interpretation. Ages of the remaining moraine boulders featured by F5a in concert with the age of FMB-19-12 of F5b correlate with the moraine age of J5 at Jamtal. The Fimbatal geochronology hence makes a case for two closely spaced stable ice margins toward the end of the YD. 3 Discussion Boulder ages in both valleys fall into three periods: (1) the Oldest Dryas to Bølling (J7), (2) the Younger Dryas (J6, J5, F5a, and F5b), and (3) the early Holocene (J3–4), and are discussed in this order. Pre-Bølling to Bølling transition The deposition of J7 (14.4 ± 1.0 ka) occurred during a period when regional climate was transitioning from stadial to interstadial conditions, i.e., from the Oldest Dryas cold phase to the Bølling warm phase. We review deglaciation of the European Alps in the millennia before the deposition of J7 to place the new moraine records at Jamtal and Fimbatal in a coherent temporal and spatial context of the Alpine LG. During the Gschnitz stadial, a well-documented post-LGM glacier readvance around 17–16 ka, the uppermost sections of the Alpine main valleys and their tributary valleys were glaciated 18 . This phase of readvance that is often associated with Heinrich event 1 in the North Atlantic 19 was followed by a period of still relatively low mean annual temperatures, but slightly increasing summer temperatures paralleling increasing solar insolation (Figures 6 a and 6 e). Despite the probably cold winters, glaciers in the Alps responded to the warmer summers after 16 ka 20 and retreated to higher elevations. Several recent studies have investigated the pace of post-LGM deglaciation in selected inner-alpine pass regions by applying surface exposure dating to bedrock sections along transects 21 – 27 . Results indicate that major ice transfluence zones, for instance, the Gotthard, the Grimsel, and the Simplon passes became ice-free between ca. 16 and 14 ka. However, local glaciers with extents that exceeded the subsequent YD glaciation may have been present until the Bølling. At Jamtal, the deposition of a moraine outboard the Egesen moraines around 14.4 ± 1.0 ka confirms the timing of ice decay reconstructed in these deglaciation studies and indicates that glacier retreat between ca. 16 ka and ca. 14 ka was discontinuous. Since LG moraines provide geomorphological evidence of discontinuous deglaciation, their identification in alpine valleys allows inferences about cold phases that interrupted the general post-LGM warming trend. The relative moraine stratigraphy of the Alpine region is based on this approach and suggests up to six more or less recognized stadials 28 , 29 , most prominently the above described ‘Gschnitz’ stadial, and the subsequent, upstream ‘Egesen’ stadial. Egesen moraines are distinct multi-ridge structures ubiquitous in high-Alpine valleys and are accepted as the morphostratigraphical equivalent of YD cooling 7 , 30 , 31 . A less conspicuous stadial, proposed as a stable ice margin in between the Gschnitz and the Egesen moraines, is the putative ‘Daun’ stadial. Daun moraines are described as recessional moraines, with less pronounced crests, often with few boulders, and sometimes affected by solifluction. They are assumed to indicate pre-Bølling glaciers that are limited to local, inner-alpine locations, being closer to the subsequent Egesen moraines than to Gschnitz. The presence of corresponding moraines in the Alps is sparse, therefore its acknowledgment as an independent stadial that is discernable at several sites across the Alps remains controversial 32 . The underrepresentation of presumable Daun moraines in geochronological studies in the Alps may be owed to their unspectacular morphology in tandem with poorer preservation, and fewer datable boulders. Nevertheless, the morphology and age of several landforms in the Alps, including the J7 moraine at Jamtal, resemble the characteristics of the Daun stadial. In a geochronological study at the Great Aletsch glacier, Schindelwig, et al. 10 investigated an ice margin indicative of glacier extents that exceed the Egesen extent. They obtained a (recalculated) age of 14.4 ± 0.7 ka (their sample VBA-7) for a boulder sitting on top of a bedrock section that deglaciated at the same time. The authors interpret the site as an LG ice margin of the Great Aletsch glacier. Böhlert, et al. 26 yielded a (recalculated) age of 15.2 ± 1.9 ka for a boulder (their sample VM7) embedded in a lateral moraine outboard the presumable Egesen moraine at Val Mulix (Switzerland) and ascribed the landform to the Daun stadial. Rolland, et al. 27 combined the analysis of proglacial lake sediments in the Argentera-Mercantour Massif with exposure dating of glacial features in the region and identified an LG moraine that was deposited ca. 14.6 ± 0.9 ka (Vens moraine, n = 3). These dated boulders and landforms, albeit limited in number, are in good agreement with the age of J7 and suggest moraine formation between ca. 16 and 14 ka in the Alps. However, any attempt to correlate J7 with the traditional Daun stadial first requires the geomorphological evaluation and dating of the type locality in the Austrian Stubai Alps 33 . Considering the age range of J7 (14.4 ±1.0), the landform could also have been deposited at the onset of the Bølling interstadial, during the Older Dryas cold snap (ca. 14 ka), or even during the subsequent Allerød interstadial (until 12.9 ka). The B-A interstadial was identified in numerous climate archives in the Northern Hemisphere 34 – 38 . Its onset around 14.6 ka is characterized by an abrupt temperature increase that induced substantial changes in environmental and vegetational conditions 39 , 40 . Summer temperatures increased by several degrees in the Alps 35 , 37 , transitioning from cooler stadial to warmer interstadial levels (Figure 6 c-d). Glaciers responded to this warming and might have retreated to the highest cirques of the Alps or disappeared completely during the B-A temperature plateau. The demise of glaciers during this interstadial appears in conflict with concurrent moraine formation of the J7 moraine outboard the subsequent Egesen ice margin. Yet, weakening of the Atlantic Meridional Overturning Circulation (AMOC) may explain centennial-scale cooling during general warming and contemporaneous stabilization or readvance of glaciers in the European Alps. Freshwater input into the North Atlantic Ocean during the deglaciation of adjacent ice sheets has the potential to decelerate or even shut down the warm northwards flowing AMOC limb and to temporarily reduce heat transport to Northern Europe 41 , 42 . Evidence of repeated freshening of ocean water between 15.8 and 12.6 ka has for instance been detected in a sediment core south of Iceland and has been linked to the deglaciation of the Laurentide ice sheet 43 . A reduction of poleward heat transport may have led to centennial-scale episodes of cooling detected in Northern and Central Europe, such as the Older Dryas and the later Gerzensee oscillations (13.3-13.0 ka) 39 . The link between the deglaciation of the Laurentide ice sheet, resulting in freshwater input into the North Atlantic, and cooling in Europe has been suggested as an explanation for abrupt centennial-scale cooling in the context of the YD-Holocene transition 44 , 45 . Moraine formation as a result of this teleconnection during the YD-Holocene transition has recently been proposed by Young, et al. 46 for the Greenland ice sheet, by Protin, et al. 8 for mountain glaciers in the French Alps, and by Braumann, et al. 9 for the Austrian Alps. Comparing the warming during the pre-Bølling to Bølling transition and during the YD-Holocene transition (Figure 6 e), we tentatively suggest brief episodes of an AMOC weakening and subsequent cooling in Europe. Even though the causation between Bølling warming, freshwater input into the Atlantic, and the AMOC circulation is elusive, we note that the timing of Bølling warming parallels MWP1A, a sea-level rise of about 12–22 m within a few centuries (Figure 6 b) 47 . The source of MWP1A remains under debate and has often been attributed to the Antarctic ice sheet alone 48 . However, recent sea-level fingerprinting and ice sheet modeling studies suggest that the melting of ice sheets in the Northern Hemisphere likely has contributed to massive sea-level rise at that time and may have caused centennial-scale cold lapses 49 – 51 . Both scenarios – moraine deposition prior to or during the Bølling – are plausible, but more direct age data covering that period are needed to better constrain moraine deposition and thus cooling between 16–14 ka in the European Alps. Interestingly, when comparing the (pre-)Bølling moraine age of J7 with mountain glacier records beyond the Alps, we find similar intervals of moraine formation in Norway 52 , 53 , in Patagonia 54 – 58 and New Zealand 59 , 60 , and the Himalaya region 61 . In the Southern Hemisphere, the climatic explanation for this phase of glacier advance is the Antarctic Cold Reversal (ACR; 14.5-12.7 ka), a millennial-scale cold phase documented in Antarctic ice cores 62 . The extent to which this cold phase propagated from Antarctica and the Southern Hemisphere further to the North remains controversial but we note that moraine formation indicated by J7 falls within the early phase of the ACR. Younger Dryas – Egesen moraines The next LG time slice that is captured by the new moraine chronologies of both valleys is the YD period. We interpret moraines J6 and J5 at Jamtal and F5a and F5b at Fimbatal as Egesen moraines that portray the fine structure of ice retreat during this final stadial before Holocene warming (Figure 6 e). J6 at Jamtal indicates an ice margin in the early phase of the YD. The lower J5 moraine and F5a/b at Fimbatal delimit glacier extents toward the very end of the YD. Exposure ages from these landforms confirm relative age estimates from a previous study in the Silvretta region that focused on geomorphology and stratigraphy 63 . The Egesen moraine sequence at Jamtal shows that the ice surface lowered by about 55 m from J6 (ca. 2440 m a.s.l.) to J5 (2385 m a.sl.) within a few centuries (Figure 4 c), hence supporting the hypothesis that climate conditions became gradually milder through the YD 64 . Glacier retreat with intermittent phases of glacier stabilization through the YD is observed at different places of the Northern Hemisphere 7 , 52 , 65 and coincides with slightly increasing summer temperatures (Figure 6 e) 34 , 35 , 66 . The mountain glacier record of the Southern Hemisphere indicates moraine deposition through glacier retreat during the same time interval 57 , 67 , which corroborates the gradual expansion of YD cooling towards the Southern Hemisphere 68 . Early Holocene Ice-surface lowering during the YD from J6 to J5 was rapid but the rate of glacier change during the transition from the YD to the EH was even faster. The downwasting of Jamtal glacier and its tributary Futschöl glacier during this period is best illustrated by comparing moraine segments J5 and to J3–4 (Figure 3 ). Even though the boulder ages of J5 and JAM-20-27 (J3–4) are statistically indistinguishable, the associated landforms indicate very different glacier positions ( Figure 7a-b ). J5 marks the right-lateral ice margin of the tributary (Futschöl) glacier when it still converged with the main (Jamtal) glacier. In turn, J3–4 indicates much smaller glacier extents when the main and the tributary glaciers were separated, which implies deglaciation of the valley flank within a few centuries (Figure 3 a, S2). The new early Holocene terminus of Jamtal glacier marked by JAM-20-27 (Figure 3 d) is located only around 900 m outboard the Holocene/LIA moraine ( Figure 7c ). J3–4 is interpreted as the equivalent of the right lateral early Holocene moraine set (JR3–4) that was mapped and dated in a previous study 9 , which in concert with the adjacent EH Laraintal chronology indicates moraine deposition and thus glacier stabilization ca. 11.0 ± 0.7 ka (Figures 6 f, 7b, and S1). The timing of moraine formation overlaps with the Preboreal Oscillation, a centennial-scale cold pulse in (Northern) Europe which was likely caused by AMOC weakening due to freshwater input into the Atlantic – the same mechanism that was tentatively proposed earlier for the deposition of J7 during the early Bølling ( section 3.1 ). Similar to the (pre-)Bølling and YD period, the synchronicity of mountain glacier stabilization during the EH is observed in glaciated regions of both hemispheres 46,69−72 . Silvretta glaciers probably remained outboard their subsequent LIA ice margins for the next several centuries but retreated to LIA-like configurations around 10 ka, which is shown based on a 10 Be moraine chronology from the adjacent Ochsental ( Figure 7c ) 17 . Throughout the rest of the Holocene, they oscillated inboard the 10 ka limits (e.g., Figure 7d ) with advances(s) to this position possibly during the Neoglacial and certainly during the LIA 73 . Broader relevance of the new moraine chronologies The 10 Be datasets from the Silvretta Massif are to date the most detailed cosmogenic-nuclide-based mountain glacier records in the Eastern European Alps. They pinpoint the timing of moraine formation in the region around 14.4 ± 1.0 ka, during the YD between 12.9 and 11.7 ka, and during the Early Holocene around 11.0 ± 0.7 ka 9 and around 9.9 ± 0.7 ka 17 . They allow for robust glacier reconstructions at different times during the LG and the Holocene, contribute to our understanding of the climate transitioning from glacial to interglacial conditions, and provide valuable constraints for the modeling of paleoglaciers. A comparison of the mountain glacier record on a global scale shows that glaciers in both hemispheres deposited moraines around 15–14 ka, during the YD, and during the EH. The next step is to investigate whether these similarities are coincidental, or due to large-scale climatic forcing. The reconstruction of Silvretta glaciers during recent geological periods shows their sensitive response to natural warming and places the magnitude and impact of anthropogenic climate change in a natural context. Methods Geomorphological mapping Hertl 63 , and references therein developed a relative moraine stratigraphy for the region on which this work is based. The pre-existing geomorphological maps were updated and supplemented with information gained during several field campaigns in the summers of 2018 to 2021, from remote sensing data 74 , 75 and drone imagery. Glacier reconstructions of Jamtal glacier for the Holocene including corresponding maps are presented in Braumann, et al. 9 . With this study, we extend the Jamtal glacier chronology into the LG and focus on landforms that evidence glacier oscillations during that period by mapping and dating margins outboard the Holocene moraines. Reconstructions of paleoglaciers are complemented with glaciological data of modern, annual- to decadal-scale glaciological data including observations of glacier mass balances, front variation, and ice-covered area 14,76−78 . Surface exposure dating with 10 Be When fresh quartz-containing rock surfaces are exposed to cosmic radiation, the production of the cosmogenic radionuclide 10 Be begins according to the nuclide-specific production rate (ca. 4 atoms −g −yr ). The longer a surface has been exposed, the more 10 Be accumulates 79 . Thus, the nuclide content in rock surfaces is a function of exposure time. This principle is used in the application of surface exposure dating to glacial landforms. A moraine boulder that is sampled for 10 Be analysis has ideally been eroded from bedrock beneath the glacier, has then been transported sub- or englacially, and has finally been deposited on a moraine crest that marks a stable ice margin. It has therefore not been exposed to cosmic radiation before its deposition on the moraine so that its radionuclide inventory is ‘zeroed’. If these assumptions are true, the 10 Be inventory measured in a rock surface after exposure will produce an age that reflects the boulder’s melt out of glacial ice, or in other words, the onset of ice retreat, hence warming. Rock samples were collected using an electric saw and hammer and chisel. The sample location was measured using a hand-held GPS device. Strike and dip angles of sampled rock surfaces were quantified using a geological compass. Samples were preferably collected from boulder tops at windswept locations to minimize shielding effects due to snow and/or sediment cover. We avoided surfaces that were affected by exfoliation and prioritized boulder locations with striations preserved on the surface, which is indicative of low postglacial erosion. For more details on our sample selection criteria, we refer to Braumann, et al. 17 ’s supplement, their Table S1. Mechanical sample preparation was accomplished at the Department of Lithospheric Research of the University of Vienna and at the Lamont-Doherty Earth Observatory (LDEO). Whole-rock samples were crushed to grain sizes between 63 and 500 µg using a mill or a jaw crusher. Mineral separation strategies included magnetic separation, boiling with phosphoric acid, froth flotation, density separation and repeated (>3) leaches with hydrofluoric acid and nitric acid at concentrations between 1% and 5% 80 . Purified quartz yields, the target mineral for 10 Be extraction, ranged from 1.1–11.3% ( Table S1 ). Samples were processed in four batches ( Table S2 ) with quartz weights ranging from 4.5939 g to 42.9287 g (Table 1 ). All samples were spiked with the LDEO 9 Be carrier (#7) made of deep-mine beryl which has a concentration of approximately 1000 ppm. The extraction of 10 Be was accomplished following the LDEO protocol described in LDEO 81 . Isotope ratios in samples ( 10 Be/ 9 Be) were measured at the Center for Accelerator Mass Spectrometry (CAMS) facility, Lawrence Livermore National Laboratory (LLNL) using the 07KNDSTD3110 standard with a 10 Be/ 9 Be ratio of 2.85 x 10 −12 82 . Exposure age calculations including statistical outlier identification (Χ 2 test) were performed using the online calculator formerly known as the CRONUS-Earth online calculator v3 83 . We used the local ‘Swiss’ production rate 84 and chose the time-dependent ‘Lm’ scaling scheme 85 . In the data presentation and discussion, we distinguish between exposure ages of individual boulders and moraine ages. Boulder ages are reported with 1σ analytical uncertainties and a 1 % error on the carrier concentration, but without uncertainties on the production rate as this source of uncertainty is constant for all boulders sampled from the same area. For moraine ages (n ≥ 3), the production rate error is propagated in quadrature to analytical and carrier uncertainties to allow the correlation of robust landform ages with moraine records from other regions. Declarations Acknowledgements This study was sponsored by inatura Museum GmbH and is based upon work supported by the National Science Foundation under grant no. NSF-1853881. SMB is a recipient of a DOC Fellowship of the Austrian Academy of Sciences (OeAW) at the Institute of Applied Geology, University of Natural Resources and Life Sciences (BOKU) Vienna. For research visits at the Lamont-Doherty Earth Observatory (LDEO) of Columbia University, SMB received a Marietta Blau scholarship sponsored by OeAD GmbH, a Marshall Plan scholarship provided by the Austrian Marshall Plan Foundation and financial support from BOKU’s ‘Transitions to Sustainability’ (T2S) doctoral school. SMB thanks the LDEO cosmogenic nuclide laboratory staff Roseanne Schwartz and Jean Hanley for advice during sample processing and Alan J. Hidy at CAMS-LLNL for 10 Be sample analysis. SMB is grateful to Dominik Blasenbauer for assistance in the field, and to Allie Balter-Kennedy for helpful discussions on the topic of this manuscript. Author Contribution SMB and JMS designed the study. All authors carried out field work. SMB accomplished cosmogenic nuclide sample preparation and age calculation. SMB wrote the manuscript and prepared the figures. All authors made substantial contributions to the data interpretation and revised and edited the manuscript. Data availability All analytical information associated with cosmogenic nuclide measurements is listed in the tables in the Supplement and will be made available via the ICE-D Alpine database ( http://alpine.ice-d.org/ ). References 1 Huston, A., Siler, N., Roe, G. H., Pettit, E. & Steiger, N. J. Understanding drivers of glacier-length variability over the last millennium. The Cryosphere 15 , 1645-1662, doi:10.5194/tc-15-1645-2021 (2021). 2 Oerlemans, J. Extracting a climate signal from 169 glacier records. Science 308 , 675-677 (2005). 3 IPCC. Climate Change 2021: The Physical Science Basis. Contribution of Working Group I to the Sixth Assessment Report of the Intergovernmental Panel on Climate Change. (2021). 4 Hock, R. et al. in IPCC Special Report on the Ocean and Cryosphere in a Changing Climate (eds H.-O. Pörtner et al.) 131-202 (IPCC - Intergovernmental Panel on Climate Change, 2019). 5 Salcher, B., Prasicek, G., Baumann, S. & Kober, F. Alpine relief limited by glacial occupation time. Geology 49 , 1209-1213, doi:10.1130/G48639.1 (2021). 6 Cunningham, M. T., Stark, C. P., Kaplan, M. R. & Schaefer, J. M. Glacial limitation of tropical mountain height. Earth Surf Dynam 7 , 147-169, doi:10.5194/esurf-7-147-2019 (2019). 7 Ivy-Ochs, S. Glacier Variations in the European Alps at the End of the Last Glaciation. Cuad Investig Geogr 41 , 295-315, doi:10.18172/cig.2750 (2015). 8 Protin, M. et al. Millennial‐scale deglaciation across the European Alps at the transition between the Younger Dryas and the Early Holocene – evidence from a new cosmogenic nuclide chronology. Boreas 50 , 671–685, doi:10.1111/bor.12519 (2021). 9 Braumann, S. M. et al. Early Holocene cold snaps and their expression in the moraine record of the eastern European Alps. Clim. Past 17 , 2451-2479, doi:10.5194/cp-17-2451-2021 (2021). 10 Schindelwig, I., Akcar, N., Kubik, P. W. & Schlüchter, C. Lateglacial and early Holocene dynamics of adjacent valley glaciers in the Western Swiss Alps. J Quaternary Sci 27 , 114-124, doi:10.1002/jqs.1523 (2012). 11 Schimmelpfennig, I. et al. Holocene glacier culminations in the Western Alps and their hemispheric relevance. Geology 40 , 891-894, doi:10.1130/G33169.1 (2012). 12 Friebe, G. Geologie der österreichischen Bundesländer - Vorarlberg. 174 (Verlag der Geologischen Bundesanstalt, 2007). 13 Fuchs, G. & Oberhauser, R. 170 Galtür. (1990). 14 Fischer, A., Schwaizer, G., Seiser, B., Helfricht, K. & Stocker-Waldhuber, M. High-resolution inventory to capture glacier disintegration in the Austrian Silvretta. Cryosphere 15 , 4637-4654 (2021). 15 Nicolussi, K. & Patzelt, G. Discovery of early-Holocene wood and peat on the forefield of the Pasterze Glacier, Eastern Alps, Austria. Holocene 10 , 191-199, doi:10.1191/095968300666855842 (2000). 16 Patzelt, G. Das Bunte Moor in der Oberfernau (Stubaier Alpen, Tirol) – Eine neu bearbeitete Schlüsselstelle für die Kenntnis der nacheiszeitlichen Gletscherschwankungen der Ostalpen. Jahrbuch der Geologischen Bundesanstalt Band 156 , 97-107 (2016). 17 Braumann, S. M. et al. Holocene glacier change in the Silvretta Massif (Austrian Alps) constrained by a new Be-10 chronology, historical records and modern observations. Quaternary Sci Rev 245 , doi:10.1016/j.quascirev.2020.106493 (2020). 18 Ivy-Ochs, S., Kerschner, H., Kubik, P. W. & Schlüchter, C. Glacier response in the European Alps to Heinrich Event 1 cooling: the Gschnitz stadial. J Quaternary Sci 21 , 115-130, doi:10.1002/jqs.955 (2006). 19 Heinrich, H. Origin and Consequences of Cyclic Ice Rafting in the Northeast Atlantic Ocean During the Past 130,000 Years. Quaternary Res 29 , 142-152, doi:10.1016/0033-5894(88)90057-9 (1988). 20 Schmidt, R., Weckstrom, K., Lauterbach, S., Tessadri, R. & Huber, K. North Atlantic climate impact on early late-glacial climate oscillations in the south-eastern Alps inferred from a multi-proxy lake sediment record. J Quaternary Sci 27 , 40-50, doi:10.1002/jqs.1505 (2012). 21 Dielforder, A. & Hetzel, R. The deglaciation history of the Simplon region (southern Swiss Alps) constrained by Be-10 exposure dating of ice-molded bedrock surfaces. Quaternary Sci Rev 84 , 26-38, doi:10.1016/j.quascirev.2013.11.008 (2014). 22 Hippe, K. et al. Chronology of Lateglacial ice flow reorganization and deglaciation in the Gotthard Pass area, Central Swiss Alps, based on cosmogenic Be-10 and in situ C-14. Quat Geochronol 19 , 14-26, doi:10.1016/j.quageo.2013.03.003 (2014). 23 Wirsig, C., Zasadni, J., Christl, M., Akcar, N. & Ivy-Ochs, S. Dating the onset of LGM ice surface lowering in the High Alps. Quaternary Sci Rev 143 , 37-50 (2016). 24 Kelly, M. A., Ivy-Ochs, S., Kubik, P. W., von Blanckenburg, F. & Schluchter, C. Chronology of deglaciation based on Be-10 dates of glacial erosional features in the Grimsel Pass region, central Swiss Alps. Boreas 35 , 634-643 (2006). 25 Wölfler, A., Hampel, A., Dielforder, A., Hetzel, R. & Glotzbach, C. LGM ice extent and deglaciation history in the Gurktal and Lavantal Alps (eastern European Alps): first constraints from 10Be surface exposure dating of glacially polished quartz veins. J Quaternary Sci Online Version of Record before inclusion in an issue , doi:10.1002/jqs.3399 (2021). 26 Böhlert, R. et al. Application of a combination of dating techniques to reconstruct the Lateglacial and early Holocene landscape history of the Albula region (eastern Switzerland). Geomorphology 127 , 1-13 (2011). 27 Rolland, Y. et al. Deglaciation history at the Alpine-Mediterranean transition (Argentera-Mercantour, SW Alps) from Be-10 dating of moraines and glacially polished bedrock. Earth Surf Proc Land 45 , 393-410 (2020). 28 Maisch, M. Zur Gletscher- und Klimageschichte des alpinen Spätglazials. Geographica Helvetica 37 , 93-104, doi:10.5169/seals-58303 (1982). 29 Kerschner, H. in Klimawandel in Österreich: Die letzten 20.000 Jahre ... und ein Blick voraus Vol. 6 alpine space – man & environment (eds R. Schmidt, C. Matulla, & R. Psenner) 5-26 (Innsbruck University Press, 2009). 30 Federici, P. R. et al. Exposure age dating and Equilibrium Line Altitude reconstruction of an Egesen moraine in the Maritime Alps, Italy. Boreas 37 , 245-253, doi:10.1111/j.1502-3885.2007.00018.x (2008). 31 Kelly, M. A., Kubik, P. W., Von Blanckenburg, F. & Schlüchter, C. Surface exposure dating of the Great Aletsch Glacier Egesen moraine system, western Swiss Alps, using the cosmogenic nuclide Be-10. J Quaternary Sci 19 , 431-441, doi:10.1002/jqs.854 (2004). 32 Reitner, J. M., Ivy-Ochs, S., Drescher-Schneider, R., Hajdas, I. & Linner, M. Reconsidering the current stratigraphy of the Alpine Lateglacial: Implications of the sedimentary and morphological record of the Lienz area (Tyrol/Austria). E&G Quaternary Sci. J. 65 , 113-144, doi:10.3285/eg.65.2.02 (2016). 33 Heuberger, H. Die Alpengletscher im Spät- und Postglazial. Eiszeitalter und Gegenwart 19 , 270-275 (1968). 34 Lauterbach, S. et al. Environmental responses to Lateglacial climatic fluctuations recorded in the sediments of pre-Alpine Lake Mondsee (northeastern Alps). J Quaternary Sci 26 , 253-267 (2011). 35 Heiri, O. et al. Palaeoclimate records 60-8 ka in the Austrian and Swiss Alps and their forelands. Quaternary Sci Rev 106 , 186-205, doi:10.1016/j.quascirev.2014.05.021 (2014). 36 Rasmussen, S. O. et al. A stratigraphic framework for abrupt climatic changes during the Last Glacial period based on three synchronized Greenland ice-core records: refining and extending the INTIMATE event stratigraphy. Quaternary Sci Rev 106 , 14-28, doi:10.1016/j.quascirev.2014.09.007 (2014). 37 Li, H. Y., Spotl, C. & Cheng, H. A high-resolution speleothem proxy record of the Late Glacial in the European Alps: extending the NALPS19 record until the beginning of the Holocene. J Quaternary Sci 36 , 29-39 (2021). 38 Kruger, S. & Damrath, M. In search of the Bolling-Oscillation: a new high resolution pollen record from the locus classicus Lake Bolling, Denmark. Veg Hist Archaeobot 29 , 189-211 (2020). 39 Ammann, B. et al. Vegetation responses to rapid warming and to minor climatic fluctuations during the Late-Glacial Interstadial (GI-1) at Gerzensee (Switzerland). Palaeogeogr Palaeocl 391 , 40-59, doi:10.1016/j.palaeo.2012.07.010 (2013). 40 Brisset, E. et al. Lateglacial/Holocene environmental changes in the Mediterranean Alps inferred from lacustrine sediments. Quaternary Sci Rev 110 , 49-71 (2015). 41 Broecker, W. S. The Great Ocean Conveyor. Oceanography 4 , 79-89, doi:10.5670/oceanog.1991.07 (1991). 42 McManus, J. F., Francois, R., Gherardi, J. M., Keigwin, L. D. & Brown-Leger, S. Collapse and rapid resumption of Atlantic meridional circulation linked to deglacial climate changes. Nature 428 , 834-837, doi:10.1038/nature02494 (2004). 43 Thornalley, D. J. R., McCave, I. N. & Elderfield, H. Freshwater input and abrupt deglacial climate change in the North Atlantic. Paleoceanography 25 , PA1201, doi:10.1029/2009PA001772 (2010). 44 Bjorck, S., Rundgren, M., Ingolfsson, O. & Funder, S. The Preboreal oscillation around the Nordic Seas: terrestrial and lacustrine responses. J Quaternary Sci 12 , 455-465 (1997). 45 Hald, M. & Hagen, S. Early preboreal cooling in the Nordic seas region triggered by meltwater. Geology 26 , 615-618 (1998). 46 Young, N. E. et al. Deglaciation of the Greenland and Laurentide ice sheets interrupted by glacier advance during abrupt coolings. Quaternary Sci Rev 229 , 106091, doi:10.1016/j.quascirev.2019.106091 (2020). 47 Lambeck, K., Rouby, H., Purcell, A., Sun, Y. Y. & Sambridge, M. Sea level and global ice volumes from the Last Glacial Maximum to the Holocene. P Natl Acad Sci USA 111 , 15296-15303, doi:10.1073/pnas.1411762111 (2014). 48 Mitrovica, J. X., Gomez, N. & Clark, P. U. The Sea-Level Fingerprint of West Antarctic Collapse. Science 323 , 753-753, doi:10.1126/science.1166510 (2009). 49 Lin, Y. et al. A reconciled solution of Meltwater Pulse 1A sources using sea-level fingerprinting. Nat Commun 12 , 2015, doi:10.1038/s41467-021-21990-y (2021). 50 Ivanovic, R. F., Gregoire, L. J., Wickert, A. D., Valdes, P. J. & Burke, A. Collapse of the North American ice saddle 14,500 years ago caused widespread cooling and reduced ocean overturning circulation. Geophys Res Lett 44 , 383-392, doi:10.1002/2016gl071849 (2017). 51 Menviel, L., Timmermann, A., Timm, O. E. & Mouchet, A. Deconstructing the Last Glacial termination: the role of millennial and orbital-scale forcings. Quaternary Sci Rev 30 , 1155-1172, doi:10.1016/j.quascirev.2011.02.005 (2011). 52 Wittmeier, H. E. et al. Late Glacial mountain glacier culmination in Arctic Norway prior to the Younger Dryas. Quaternary Sci Rev 245 , doi:10.1016/j.quascirev.2020.106461 (2020). 53 Briner, J. P., Svendsen, J. I., Mangerud, J., Lohne, O. S. & Young, N. E. A Be-10 chronology of south-western Scandinavian Ice Sheet history during the Lateglacial period. J Quaternary Sci 29 , 370-380, doi:10.1002/jqs.2710 (2014). 54 Glasser, N. F. et al. Cosmogenic nuclide exposure ages for moraines in the Lago San Martin Valley, Argentina. Quaternary Res 75 , 636-646, doi:10.1016/j.yqres.2010.11.005 (2011). 55 Garcia, J. L. et al. Glacier expansion in southern Patagonia throughout the Antarctic cold reversal. Geology 40 , 859-862, doi:10.1130/G33164.1 (2012). 56 Moreno, P. I. et al. Renewed glacial activity during the Antarctic cold reversal and persistence of cold conditions until 11.5 ka in southwestern Patagonia. Geology 37 , 375-378, doi:10.1130/G25399a.1 (2009). 57 Sagredo, E. A. et al. Trans-pacific glacial response to the Antarctic Cold Reversal in the southern mid-latitudes. Quaternary Sci Rev 188 , 160-166, doi:10.1016/j.quascirev.2018.01.011 (2018). 58 Davies, B. J., Thorndycraft, V. R., Fabel, D. & Martin, J. R. V. Asynchronous glacier dynamics during the Antarctic Cold Reversal in central Patagonia. Quaternary Sci Rev 200 , 287-312, doi:10.1016/j.quascirev.2018.09.025 (2018). 59 Putnam, A. E. et al. Glacier advance in southern middle-latitudes during the Antarctic Cold Reversal. Nat Geosci 3 , 700-704, doi:10.1038/Ngeo962 (2010). 60 Putnam, A. E. et al. Warming and glacier recession in the Rakaia valley, Southern Alps of New Zealand, during Heinrich Stadial 1. Earth Planet Sc Lett 382 , 98-110, doi:10.1016/j.epsl.2013.09.005 (2013). 61 Lee, S. Y. et al. Late Quaternary glaciation in the Nun-Kun massif, northwestern India. Boreas 43 , 67-89, doi:10.1111/bor.12022 (2014). 62 Lemieux-Dudon, B. et al. Consistent dating for Antarctic and Greenland ice cores. Quaternary Sci Rev 29 , 8-20, doi:10.1016/j.quascirev.2009.11.010 (2010). 63 Hertl, A. Untersuchungen zur spätglazialen Gletscher- und Klimageschichte der Österreichischen Silvrettagruppe, Leopold-Franzens-Universität Innsbruck, (2001). 64 Alley, R. B. The Younger Dryas cold interval as viewed from central Greenland. Quaternary Sci Rev 19 , 213-226, doi:10.1016/S0277-3791(99)00062-1 (2000). 65 Briner, J. P. et al. Using in situ cosmogenic Be-10, C-14, and Al-26 to decipher the history of polythermal ice sheets on Baffin Island, Arctic Canada. Quat Geochronol 19 , 4-13, doi:10.1016/j.quageo.2012.11.005 (2014). 66 Buizert, C. et al. Greenland-Wide Seasonal Temperatures During the Last Deglaciation. Geophys Res Lett 45 , 1905-1914, doi:10.1002/2017gl075601 (2018). 67 Kaplan, M. R. et al. Glacier retreat in New Zealand during the Younger Dryas stadial. Nature 467 , 194-197, doi:10.1038/nature09313 (2010). 68 Cheng, H. et al. Timing and structure of the Younger Dryas event and its underlying climate dynamics. P Natl Acad Sci USA 117 , 23408-23417, doi:10.1073/pnas.2007869117 (2020). 69 Putnam, A. E. et al. Regional climate control of glaciers in New Zealand and Europe during the pre-industrial Holocene. Nat Geosci 5 , 627-630, doi:10.1038/NGEO1548 (2012). 70 Glasser, N. F., Harrison, S., Schnabel, C., Fabel, D. & Jansson, K. N. Younger Dryas and early Holocene age glacier advances in Patagonia. Quaternary Sci Rev 58 , 7-17, doi:10.1016/j.quascirev.2012.10.011 (2012). 71 Reynhout, S. A. et al. Holocene glacier fluctuations in Patagonia are modulated by summer insolation intensity and paced by Southern Annular Mode-like variability. Quaternary Sci Rev 220 , 178-187, doi:10.1016/j.quascirev.2019.05.029 (2019). 72 Saha, S., Owen, L. A., Orr, E. N. & Caffee, M. W. High-frequency Holocene glacier fluctuations in the Himalayan-Tibetan orogen. Quaternary Sci Rev 220 , 372-400, doi:10.1016/j.quascirev.2019.07.021 (2019). 73 Fischer, A., Seiser, B., Waldhuber, M. S., Mitterer, C. & Abermann, J. Tracing glacier changes in Austria from the Little Ice Age to the present using a lidar-based high-resolution glacier inventory in Austria. Cryosphere 9 , 753-766, doi:10.5194/tc-9-753-2015 (2015). 74 Land Tirol. (Land Tirol, Innsbruck, 2021). 75 swisstopo. (Bundesamt für Landestopografie, Wabern, 2021). 76 Hartl, L., Felbauer, L., Schwaizer, G. & Fischer, A. Small-scale spatial variability in bare-ice reflectance at Jamtalferner, Austria. Cryosphere 14 , 4063-4081 (2020). 77 Fischer, A., Fickert, T., Schweizer, G., Patzelt, G. & Gross, G. Vegetation dynamics in Alpine glacier forelands tackled from space. Sci Rep-Uk 9 , 13918, doi:10.1038/s41598-019-50273-2 (2019). 78 WGMS. Global Glacier Change Bulletin No. 4 (2018–2019). Global Glacier Change Bulletin, doi:doi:10.5904/wgms-fog-2021-05 (2021). 79 Lal, D. In situ-produced Cosmogenic Isotopes in Terrestrial Rocks. Annu Rev Earth Pl Sc 16 , 355-388, doi:10.1146/annurev.ea.16.050188.002035 (1988). 80 LDEO. Separation and Purifiation of Quartz from Whole Rock. 8 (2012). 81 LDEO. Extraction of Beryllium from Quartz. 19 (2012). 82 Nishiizumi, K. et al. Absolute calibration of Be-10 AMS standards. Nucl Instrum Meth B 258 , 403-413, doi:10.1016/j.nimb.2007.01.297 (2007). 83 Balco, G., Stone, J. O., Lifton, N. A. & Dunai, T. J. A complete and easily accessible means of calculating surface exposure ages or erosion rates from Be-10 and Al-26 measurements. Quat Geochronol 3 , 174-195, doi:10.1016/j.quageo.2007.12.001 (2008). 84 Claude, A. et al. The Chironico landslide (Valle Leventina, southern Swiss Alps): age and evolution. Swiss J Geosci 107 , 273-291, doi:10.1007/s00015-014-0170-z (2014). 85 Stone, J. O. Air pressure and cosmogenic isotope production. J Geophys Res-Sol Ea 105 , 23753-23759, doi:10.1029/2000jb900181 (2000). 86 Linsbauer, A. et al. The New Swiss Glacier Inventory SGI2016: From a Topographical to a Glaciological Dataset. Frontiers in Earth Science 9 , doi:10.3389/feart.2021.704189 (2021). 87 Moran, A. P., Kerschner, H. & Ivy-Ochs, S. Redating the moraines in the Kromer Valley (Silvretta Mountains) - New evidence for an early Holocene glacier advance. Holocene 26 , 655-664, doi:10.1177/0959683615612571 (2016). 88 Auer, I. et al. HISTALP - historical instrumental climatological surface time series of the Greater Alpine Region. Int J Climatol 27 , 17-46, doi:10.1002/joc.1377 (2007). 89 BMLRT. Vol. 2009-2018 (BMLRT, Vienna, 2021). 90 MacFarling Meure, C. et al. Law Dome CO2, CH4 and N2O ice core records extended to 2000 years BP. Geophys Res Lett 33 , L14810, doi:10.1029/2006GL026152 (2006). 91 NOAA Global Monitoring Laboratory. (NOAA Research, 2021). 92 Berger, A. & Loutre, M. F. in Supplement to: Berger, A; Loutre, M-F (1991): Insolation values for the climate of the last 10 million of years. Quaternary Science Reviews, 10(4), 297-317, https://doi.org/10.1016/0277-3791(91)90033-Q (PANGAEA, 1999). 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Braumann","email":"data:image/png;base64,iVBORw0KGgoAAAANSUhEUgAAAZAAAAAyAQMAAABI0h/eAAAABlBMVEX///8AAABVwtN+AAAACXBIWXMAAA7EAAAOxAGVKw4bAAABEElEQVRIiWNgGAWjYJACCSBOgHHkDBjYSNRijNCCRyuKlsQNhLTIt589eLuihiHPvP2M6YafO+6kb2dvS5NgqLFj4J/fgFWLwZm8ZMszxxiKZc7kmN3sPfMsd2fPsWMSDMeSGSSOYbfFgCHHTLKBjSFxBpBxg7ftcO6GG+ltEgxsBxgYcGiR738D1PIPqIX/jdnNv22H0w3AWv4dYJDHoYXhBtCWxjagFokcs9tAWxIMbqQdk2BsO8BggMthN94YWzb2SRRLSDwruy3bdtgQ6Jdki8S+ZB7DYwk4HJZjeLPhm02eBH/ytptv2w7Lm7O3Gd748M1OTu7wARwuAwMJND7QfB586kfBKBgFo2AU4AcAo5hd+AnvOrkAAAAASUVORK5CYII=","orcid":"","institution":"University of Natural Resources and Life Sciences (BOKU)","correspondingAuthor":true,"submittingAuthor":false,"prefix":"","firstName":"Sandra","middleName":"M.","lastName":"Braumann","suffix":""},{"id":83711884,"identity":"3983239c-c95f-4ff9-b289-c2714151e946","order_by":1,"name":"Joerg M. Schaefer","email":"","orcid":"","institution":"Lamont-Doherty Earth Observatory of Columbia University","correspondingAuthor":false,"submittingAuthor":false,"prefix":"","firstName":"Joerg","middleName":"M.","lastName":"Schaefer","suffix":""},{"id":83711885,"identity":"d56e06f2-1fde-49c9-8b74-20a439212da8","order_by":2,"name":"Stephanie Neuhuber","email":"","orcid":"","institution":"University of Natural Resources and Life Sciences (BOKU)","correspondingAuthor":false,"submittingAuthor":false,"prefix":"","firstName":"Stephanie","middleName":"","lastName":"Neuhuber","suffix":""},{"id":83711886,"identity":"34192561-ce12-47a1-b961-fa84e0edadd3","order_by":3,"name":"Markus Fiebig","email":"","orcid":"","institution":"University of Natural Resources and Life Sciences (BOKU)","correspondingAuthor":false,"submittingAuthor":false,"prefix":"","firstName":"Markus","middleName":"","lastName":"Fiebig","suffix":""}],"badges":[],"createdAt":"2022-02-02 14:29:14","currentVersionCode":1,"declarations":"","doi":"10.21203/rs.3.rs-1321188/v1","doiUrl":"https://doi.org/10.21203/rs.3.rs-1321188/v1","draftVersion":[],"editorialEvents":[{"content":"https://doi.org/10.1038/s41598-022-12477-x","type":"published","date":"2022-06-13T00:00:00+00:00"}],"editorialNote":"","failedWorkflow":false,"files":[{"id":18326522,"identity":"0ce48c68-638c-48b8-8eeb-f8012289ce6e","added_by":"auto","created_at":"2022-02-17 15:14:51","extension":"png","order_by":1,"title":"Figure 1","display":"","copyAsset":false,"role":"figure","size":1114518,"visible":true,"origin":"","legend":"\u003cp\u003eLocation of study sites.\u003cstrong\u003e (a.)\u003c/strong\u003e Overview of the European Alps (yellow line); red star symbol marks Silvretta region, a glaciated area at the transition zone between the Western and the Eastern Alps. \u003cstrong\u003e(b.) \u003c/strong\u003eInvestigated valleys in the north-facing part of the Silvretta region. Ice extents during the Little Ice Age (LIA) are depicted in pink, modern glacier extents indicated with blue signature (glacier extents of 2016 for Switzerland CH; glacier extents 2015 for Austria AUT) \u003csup\u003e73,86\u003c/sup\u003e. DEMs ©swisstopo, ©Land Tirol, and ©Land Vorarlberg. Valleys with previously published \u003csup\u003e10\u003c/sup\u003eBe moraine records from West to East: Kromertal (KRO) and Klostertal (KL) #1: Moran, et al. \u003csup\u003e87\u003c/sup\u003e, Ochsental (OcG-GrK) #2: Braumann, et al. \u003csup\u003e17\u003c/sup\u003e, Jamtal (JAM) with tributary valley Futschöltal (F) and Laraintal (LAR) #3: Braumann, et al. \u003csup\u003e9\u003c/sup\u003e and #4: this study, FMB – Fimbatal (#4: this study).\u003c/p\u003e","description":"","filename":"fig1.png","url":"https://assets-eu.researchsquare.com/files/rs-1321188/v1/e81c90079cc35c197d423ad5.png"},{"id":18326877,"identity":"1aa3108a-4430-4b3f-8619-7f6df4c3dab8","added_by":"auto","created_at":"2022-02-17 15:17:51","extension":"png","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":132879,"visible":true,"origin":"","legend":"\u003cp\u003eResponse of Jamtal glacier to greenhouse gas emissions and rising temperatures over the past decades.\u003cstrong\u003e (a.)\u003c/strong\u003e Mass balance record of Jamtal glacier (1989-2020 CE) with negative values ranging between -62 mm water equivalent (w.e.) (2000 CE) and -2276 mm water equivalent (2018 CE)\u0026nbsp;\u003csup\u003e78\u003c/sup\u003e.\u003cstrong\u003e (b.) \u003c/strong\u003eFront variation of Jamtal glacier (1891-2019) showing retreat of ca. 1.5 km since 1891 CE \u003csup\u003e78\u003c/sup\u003e. \u003cstrong\u003e(c.) \u003c/strong\u003eMean summer temperature (grey line) at meteorological station Galtür (station number: 101949; 1587 m a.s.l.) overlain with 20 yrs low pass filter (black line) \u003csup\u003e88,89\u003c/sup\u003e. \u003cstrong\u003e(d.)\u003c/strong\u003e Mean annual atmospheric greenhouse gas concentrations (1880-2004) derived from Law Dome ice core (solid lines) \u003csup\u003e90\u003c/sup\u003e. Globally averaged marine surface annual data of CH\u003csub\u003e4\u003c/sub\u003e\u0026nbsp;(1984-2020 CE; green dashed line), CO\u003csub\u003e2\u003c/sub\u003e (1959-2020; orange dashed line), and N\u003csub\u003e2\u003c/sub\u003e0 (2001-2020; blue dashed line) provided by \u003csup\u003e91\u003c/sup\u003e.\u003c/p\u003e","description":"","filename":"fig2.png","url":"https://assets-eu.researchsquare.com/files/rs-1321188/v1/85e89dfa9806ee33eca1a513.png"},{"id":18326874,"identity":"72599779-1477-4f47-b377-5ddecade727a","added_by":"auto","created_at":"2022-02-17 15:17:51","extension":"png","order_by":3,"title":"Figure 3","display":"","copyAsset":false,"role":"figure","size":959087,"visible":true,"origin":"","legend":"\u003cp\u003ePhotographs and map of sampled valley sections at Jamtal.\u003cstrong\u003e (a.) \u003c/strong\u003eMoraine sequence (dotted lines) evidence confluence of tributary (Futschöl) glacier with the main (Jamtal) glacier during the LG. The uppermost landform J7 indicates a stable ice margin position during (Pre-)Bølling times. J6 and J5 were deposited during the YD and suggest a lowering of the ice surface of ca. 55 m from the early YD to its end. For unedited photograph, we refer to Figure S2. \u003cstrong\u003e(b.) \u003c/strong\u003eMap showing sample and landform locations at Jamtal (DEM provided by © Land Tirol). \u003cstrong\u003e(c.) \u003c/strong\u003eLateral moraine set deposited during the EH. The inner of two ridges (arrow) features boulder age JAM-20-26 and is (due to its position) several centuries younger compared to \u003cstrong\u003e(d.)\u003c/strong\u003e sample JAM-20-27 taken from the terminal section of J3-4. The statistically identical ages of J5 and JAM-20-27 suggest that the valley flank displayed in (a.) deglaciated within centuries during the YD-EH transition.\u0026nbsp;\u003c/p\u003e","description":"","filename":"fig3.png","url":"https://assets-eu.researchsquare.com/files/rs-1321188/v1/693280114906dcbf6bc946be.png"},{"id":18326527,"identity":"b4a761bb-02e1-4db9-8ebe-6e1dc50a8482","added_by":"auto","created_at":"2022-02-17 15:14:51","extension":"png","order_by":4,"title":"Figure 4","display":"","copyAsset":false,"role":"figure","size":794625,"visible":true,"origin":"","legend":"\u003cp\u003eCloseups of dated moraines\u003cstrong\u003e (a.) \u003c/strong\u003eJ7,\u003cstrong\u003e (b.)\u003c/strong\u003e J6 and \u003cstrong\u003e(d.)\u003c/strong\u003e J5 highlight different geomorphological characteristics of the three landforms. \u003cstrong\u003e(c.) \u003c/strong\u003eProfile along LG valley flank (for location see Figure 3b) indicating ice surface positions at different times during the LG.\u003c/p\u003e","description":"","filename":"fig4.png","url":"https://assets-eu.researchsquare.com/files/rs-1321188/v1/b2f77ac66f2d6ddf2bef035e.png"},{"id":18327168,"identity":"9d5ff307-1f2f-4785-aa71-0f6a24983528","added_by":"auto","created_at":"2022-02-17 15:20:51","extension":"png","order_by":5,"title":"Figure 5","display":"","copyAsset":false,"role":"figure","size":855770,"visible":true,"origin":"","legend":"\u003cp\u003ePhotograph and map of sampled valley sections at Fimbatal.\u003cstrong\u003e (a.) \u003c/strong\u003ePhotograph of F5a and F5b moraines indicating stable termini of Fimba glacier toward the end of the YD at an elevation of c. 2040 m a.s.l.; outliers are colored in gray.\u003cstrong\u003e (b.)\u003c/strong\u003e Map showing sample and landform locations at Jamtal (DEM provided by © Land Tirol).\u003c/p\u003e","description":"","filename":"fig5.png","url":"https://assets-eu.researchsquare.com/files/rs-1321188/v1/079681b546953fe1105bdcf0.png"},{"id":18327381,"identity":"1c1121f7-ee7f-4778-8b7d-b14cf797017c","added_by":"auto","created_at":"2022-02-17 15:23:51","extension":"png","order_by":6,"title":"Figure 6","display":"","copyAsset":false,"role":"figure","size":238541,"visible":true,"origin":"","legend":"\u003cp\u003eSilvretta mountain glacier records correlated with solar insolation, sea-level rise, and climate proxy records from different regions in the Northern Hemisphere.\u003cstrong\u003e (a.)\u003c/strong\u003e Insolation at 65N \u003csup\u003e92\u003c/sup\u003e gradually increases during the LG and is a natural forcing for climate warming during this period.\u003cstrong\u003e (b.)\u003c/strong\u003e Global sea-level rise due to deglaciation of the cryosphere \u003csup\u003e47\u003c/sup\u003e; note increased rate of change between 14.5 and 14 ka, and 11.4 ka onwards. \u003cstrong\u003e(c.) \u003c/strong\u003eLocal high-resolution ostracod record from lake Mondsee \u003csup\u003e34\u003c/sup\u003e. \u003cstrong\u003e(d.)\u003c/strong\u003e Chironomid-inferred summer temperature stack record for the Alpine region \u003csup\u003e35\u003c/sup\u003e. \u003cstrong\u003e(e.)\u003c/strong\u003e Summer temperatures (as driving factor for mountain glacier oscillations) from Greenland Ice Sheet (GrIS) reconstructed based on oxygen isotopes in Greenland ice cores\u0026nbsp;\u003csup\u003e66\u003c/sup\u003e. Temperatures reconstructed based on different methods and from different regions in the Northern Hemisphere agree well and capture the YD stadial as well as the two bracketing episodes of rapid climate warming, the Pre-Bølling to Bølling transition and the YD-EH transition. \u003cstrong\u003e(f.) \u003c/strong\u003eGlacier stabilization during general LG warming indicated by moraines deposited during Oldest Dryas to Bølling transition ( J7), the YD (Egesen moraines J6, J5, and F5a/b), and the EH (J3-4 and L3-4) is this study and Braumann, et al. \u003csup\u003e9\u003c/sup\u003e. By 10 ka, Silvretta glaciers have retreated to positions that resemble (subsequent) LIA extents indicated by the \u003csup\u003e10\u003c/sup\u003eBe moraine record in the adjacent Ochsental \u003csup\u003e17\u003c/sup\u003e. Moraine ages (n ≥ 3) are shown with rectangles, individual boulder ages with circles. Kernel plots of moraine ages are provided in the supplement (Figure S1). For the spatial context of the displayed \u003csup\u003e10\u003c/sup\u003eBe records, see Figure 1b and Figure 7.\u003c/p\u003e","description":"","filename":"fig6.png","url":"https://assets-eu.researchsquare.com/files/rs-1321188/v1/c4a74e8995839ba9b0cb47e2.png"},{"id":18326523,"identity":"16968b5e-399e-49c4-817c-786099cc78e0","added_by":"auto","created_at":"2022-02-17 15:14:51","extension":"png","order_by":7,"title":"Figure 7","display":"","copyAsset":false,"role":"figure","size":892803,"visible":true,"origin":"","legend":"\u003cp\u003ePossible extents of Silvretta glaciers during the\u003cstrong\u003e (a.)\u003c/strong\u003e the later YD, \u003cstrong\u003e(b.)\u003c/strong\u003e the EH, \u003cstrong\u003e(c.) \u003c/strong\u003earound 10 ka and during the LIA, and\u003cstrong\u003e (d.) \u003c/strong\u003ein 2015/16 CE. Positions of dated boulders are indicated with yellow symbols across all valleys and time slices and are published in this study (#1), in Braumann, et al. \u003csup\u003e9\u003c/sup\u003e (#2), in Moran, et al. \u003csup\u003e87\u003c/sup\u003e (#3), and in Braumann, et al. \u003csup\u003e17\u003c/sup\u003e (#4). IDs of corresponding moraines are adopted from original publications and are shown in rectangles. Ice margins positions with geochronological data available (yellow circles) are reliable. All other ice margins in (a.) and (b.) are estimates and are based on Hertl \u003csup\u003e63\u003c/sup\u003e. LIA and modern ice margins are taken from the Austrian and the Swiss glacier inventories, respectively \u003csup\u003e73,86\u003c/sup\u003e. The Jamtal moraine record in the context of previously published moraine records of the region indicates that the transition from YD to EH ice extents occurred within a few centuries.\u0026nbsp;\u003c/p\u003e","description":"","filename":"fig7.png","url":"https://assets-eu.researchsquare.com/files/rs-1321188/v1/29c253ccc90ac9aff8a0da9b.png"},{"id":25004671,"identity":"501efa90-b6c9-47ad-b4fd-242b4b785187","added_by":"auto","created_at":"2022-08-09 19:43:29","extension":"pdf","order_by":0,"title":"","display":"","copyAsset":false,"role":"manuscript-pdf","size":5282522,"visible":true,"origin":"","legend":"","description":"","filename":"manuscript.pdf","url":"https://assets-eu.researchsquare.com/files/rs-1321188/v1/5cba6b73-f690-42a7-845c-ade9969442b5.pdf"},{"id":18326529,"identity":"2f52cc7f-3f4a-4ad3-9839-00e2b70b0847","added_by":"auto","created_at":"2022-02-17 15:14:53","extension":"pdf","order_by":3,"title":"","display":"","copyAsset":false,"role":"supplement","size":21383821,"visible":true,"origin":"","legend":"","description":"","filename":"Braumannetal.SUPPLEMENTMorainesintheAustrianAlpsrecordrepeatedphasesofglacierstabilizationthroughtheLateGlacialandtheEarlyHolocene.pdf","url":"https://assets-eu.researchsquare.com/files/rs-1321188/v1/fd4c48b1e82d70551da668f3.pdf"}],"financialInterests":"No competing interests reported.","formattedTitle":"\u003cp\u003eMoraines in the Austrian Alps Record Repeated Phases of Glacier Stabilization through the Late Glacial and the Early Holocene\u003c/p\u003e","fulltext":[{"header":"1 Introduction","content":"\u003cp\u003eMountain glaciers are highly sensitive to climate variations, most importantly to changes in summer temperatures and to a lesser extent to changes in precipitation \u003csup\u003e\u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e1\u003c/span\u003e,\u003cspan citationid=\"CR2\" class=\"CitationRef\"\u003e2\u003c/span\u003e\u003c/sup\u003e. This sensitivity is evident in the accelerating deglaciation of alpine regions caused by rapid warming due to increasing greenhouse gas emissions in recent decades \u003csup\u003e\u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e3\u003c/span\u003e, chapter \u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e3\u003c/span\u003e, section \u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e3\u003c/span\u003e.\u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e3\u003c/span\u003e\u003c/sup\u003e. Deglaciation affects mountain regions in various ways, including altering the hydrological regime in these areas and downstream, impacting ecosystems, and increasing the frequency of natural hazards \u003csup\u003e\u003cspan citationid=\"CR4\" class=\"CitationRef\"\u003e4\u003c/span\u003e\u003c/sup\u003e. Improving our understanding of interactions between the climate system and the cryosphere in the past helps to project the magnitude and impact of environmental change in the future.\u003c/p\u003e \u003cp\u003eGlaciers and their shaping of many parts of the earth\u0026rsquo;s surface in the past \u003csup\u003e\u003cspan citationid=\"CR5\" class=\"CitationRef\"\u003e5\u003c/span\u003e,\u003cspan citationid=\"CR6\" class=\"CitationRef\"\u003e6\u003c/span\u003e\u003c/sup\u003e enable us to explore the climate system and how it operates with and without anthropogenic impact. Detailed geomorphological mapping and direct dating of former ice margins allow us to reconstruct glaciers across time and space and to draw conclusions about the climate conditions that drove glacier advance or retreat in the past. Here, we present ice-margin reconstructions of two glaciated valleys in the Austrian Alps, at Jamtal and Fimbatal, covering the Late Glacial (LG) and the Early Holocene (EH) \u0026ndash; a period when the climate was transitioning from a glacial to an interglacial mode.\u003c/p\u003e \u003cp\u003eLG moraines in the European Alps, especially those deposited during the Younger Dryas (YD, ca. 12.9\u0026ndash;11.7 ka) termed \u0026lsquo;Egesen\u0026rsquo; moraines, are subject to numerous geochronological studies that provide valuable insights into this last phase of prolonged cooling before Holocene warming \u003csup\u003e\u003cspan citationid=\"CR7\" class=\"CitationRef\"\u003e7\u003c/span\u003e\u003c/sup\u003e. Other periods of climate transition before and after the YD remain more controversial in terms of glacier extents and ice dynamics, for instance, the B\u0026oslash;lling-Aller\u0026oslash;d period (B-A, ca. 14.6\u0026ndash;12.9 ka) and the EH (ca. 11.7\u0026ndash;9 ka). Although glaciers were presumably much more extensive at the beginning of the B-A compared to the beginning of the EH, they were driven by a similar climatic pattern during both periods: a steep temperature increase which led to rapid deglaciation. For the period between ca. 12 and 10 ka, moraine chronologies from different places in the Alps, including data presented in this study, have shown that ice retreat and therefore warming was not linear, but was interrupted by centennial-scale cooling \u003csup\u003e\u003cspan additionalcitationids=\"CR9 CR10\" citationid=\"CR8\" class=\"CitationRef\"\u003e8\u003c/span\u003e\u0026ndash;\u003cspan citationid=\"CR11\" class=\"CitationRef\"\u003e11\u003c/span\u003e\u003c/sup\u003e. For the (pre-)B\u0026oslash;lling period, it is still unclear whether ice retreat was steady and of such magnitude that most glaciers in the European Alps retreated to the highest cirques or disappeared altogether \u003csup\u003e\u003cspan citationid=\"CR7\" class=\"CitationRef\"\u003e7\u003c/span\u003e\u003c/sup\u003e. The objective of this study is to contribute to these less resolved periods and to view climate transitions from glacial to interglacial conditions through the lens of glacial geomorphology. Therefore, we mapped moraine sequences at two alpine valleys, the Jamtal and the Fimbatal, and applied \u003csup\u003e10\u003c/sup\u003eBe surface exposure dating to selected landforms to produce direct spatial and temporal information of former ice extents in the Silvretta Massif.\u003c/p\u003e \u003cp\u003eThe Silvretta Massif is in the westernmost part of the Eastern European Alps (Figure \u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ea). The mountain range belongs to the Upper Eastern Alpine (\u0026ldquo;Oberostalpin\u0026rdquo;) tectonic unit and consists of crystalline rocks that have undergone several metamorphic events since their formation during the Precambrian \u003csup\u003e\u003cspan citationid=\"CR12\" class=\"CitationRef\"\u003e12\u003c/span\u003e\u003c/sup\u003e. Lithologies in the valleys include amphibolites, different types of metasediments, and gneisses \u003csup\u003e\u003cspan citationid=\"CR13\" class=\"CitationRef\"\u003e13\u003c/span\u003e\u003c/sup\u003e. Glaciers in the region are temperate and are sensitive to climate oscillations (Figure \u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e). Over the past 150 years, rapidly increasing greenhouse gas emissions and resulting warming have led to the melting of glacial ice across the planet. In the Silvretta region, the ice-covered area has decreased to 32 \u0026plusmn; 2 % of the extent of the Little Ice Age (LIA; ca. 1250\u0026ndash;1850 CE) in the reference years 2017/2018 (Figure \u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003eb) \u003csup\u003e\u003cspan citationid=\"CR14\" class=\"CitationRef\"\u003e14\u003c/span\u003e\u003c/sup\u003e. Jamtal glacier \u0026ndash; the main ice body at Jamtal \u0026ndash; has retreated to a position ca. 2 km upstream from the LIA maximum. In 2018, it covered approximately 2.8 km\u0026sup2; with its terminus at an altitude of ca. 2410 m a.s.l. Glaciers at Fimbatal have largely disappeared today with only a few small patches of dead ice left in the uppermost sections of the valley (Figure \u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003eb). In deglaciated sections of both valleys, sequences of lateral and terminal moraines are preserved that evidence stable ice margins of the past and promise insights into periods when climate conditions were favorable for larger glaciers (Figures \u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e3\u003c/span\u003e-\u003cspan refid=\"Fig6\" class=\"InternalRef\"\u003e5\u003c/span\u003e, \u003cb\u003eFigure S2\u003c/b\u003e).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e"},{"header":"2 Results","content":"\u003cp\u003eA total of 15 rock samples were collected from moraines at Jamtal (n=9) and Fimbatal (n=6). Ages are stratigraphically in order and are presented from old to young, beginning with the Jamtal (JAM) record, followed by the Fimbatal (FMB) record. \u003csup\u003e10\u003c/sup\u003eBe analytical data and boulder ages are presented in Table \u003cspan class=\"InternalRef\"\u003e1\u003c/span\u003e and in Figures \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003e-\u003cspan class=\"InternalRef\"\u003e5\u003c/span\u003e as well as in the supplement (\u003cstrong\u003eTables S1 and S2, section S4\u003c/strong\u003e).\u003c/p\u003e\n\u003cdiv class=\"gridtable\"\u003e\u0026nbsp;\u003ctable border=\"1\" id=\"Tab1\"\u003e\n \u003ccaption language=\"En\"\u003e\n \u003cdiv class=\"CaptionNumber\"\u003eTable 1\u003c/div\u003e\n \u003cdiv class=\"CaptionContent\"\u003e\n \u003cp\u003e\u003csup\u003e10\u003c/sup\u003eBe analytical data and corresponding exposure ages of Jamtal samples. Samples were analyzed at the CAMS-LLNL. All samples were measured against the 07KNSTD3110 standard with a ratio of 2.85 x 10\u003csup\u003e\u0026minus;12 82\u003c/sup\u003e. One to two procedural blanks were processed with each batch of samples with ratios ranging from 2.3 to 8.4 x 10\u003csup\u003e\u0026minus;16\u003c/sup\u003e (Table S2). The \u003csup\u003e10\u003c/sup\u003eBe background contaminations measured in the blanks were subtracted from the samples. Exposure ages were calculated with the calculator formerly known as CRONUS-Earth online calculator v3; \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e83\u003c/span\u003e\u003c/sup\u003e, using the Swiss \u003csup\u003e10\u003c/sup\u003eBe production rate \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e84\u003c/span\u003e\u003c/sup\u003e and choosing the \u0026lsquo;Lm\u0026rsquo; scaling scheme. Ages are calculated relative to the sampling year denoted by the first number in the sample ID and are rounded to the nearest 10 years. Uncertainties of boulder ages include the 1\u0026sigma; analytical error and a 1% uncertainty on the carrier concentration.\u003c/p\u003e\n \u003c/div\u003e\n \u003c/caption\u003e\n \u003ccolgroup cols=\"22\"\u003e\u003c/colgroup\u003e\n \u003cthead\u003e\n \u003ctr\u003e\n \u003cth align=\"left\"\u003e\u0026nbsp;\u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cp\u003eSample ID\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cp\u003eLatitude\u003c/p\u003e\n \u003cp\u003e[DD]\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cp\u003eLongitude\u003c/p\u003e\n \u003cp\u003e[DD]\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cp\u003eElevation\u003c/p\u003e\n \u003cp\u003e[m a.s.l.]\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cp\u003eAv.\u003c/p\u003e\n \u003cp\u003ethickness\u003c/p\u003e\n \u003cp\u003e[cm]\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cp\u003eShielding factor\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cp\u003eQuartz mass\u003c/p\u003e\n \u003cp\u003e[g]\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cp\u003e\u003csup\u003e9\u003c/sup\u003eBe\u003c/p\u003e\n \u003cp\u003ecarrier\u003c/p\u003e\n \u003cp\u003e[g]\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\" colspan=\"4\"\u003e\n \u003cp\u003e\u003csup\u003e10\u003c/sup\u003eBe/\u003csup\u003e9\u003c/sup\u003eBe ratio\u003c/p\u003e\n \u003cp\u003e\u0026plusmn;1\u0026sigma; analytical unc.\u003c/p\u003e\n \u003cp\u003e(10\u003csup\u003e\u0026minus;14\u003c/sup\u003e)\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\" colspan=\"3\"\u003e\n \u003cp\u003e\u003csup\u003e10\u003c/sup\u003eBe atoms\u003c/p\u003e\n \u003cp\u003e\u0026plusmn;1\u0026sigma; analytical unc.\u003c/p\u003e\n \u003cp\u003e[atoms]\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\" colspan=\"3\"\u003e\n \u003cp\u003e\u003csup\u003e10\u003c/sup\u003eBe conc.\u003c/p\u003e\n \u003cp\u003e\u0026plusmn;1\u0026sigma; analytical unc.\u003c/p\u003e\n \u003cp\u003e[atoms/g qtz]\u003c/p\u003e\n \u003c/th\u003e\n \u003cth align=\"left\" colspan=\"3\"\u003e\n \u003cp\u003e\u003csup\u003e10\u003c/sup\u003eBe exposure age\u003c/p\u003e\n \u003cp\u003e\u0026plusmn;1\u0026sigma; analytical unc. and carrier unc.\u003c/p\u003e\n \u003cp\u003e[yrs]\u003c/p\u003e\n \u003c/th\u003e\n \u003c/tr\u003e\n \u003c/thead\u003e\n \u003ctbody\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eF5b\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eFMB-18-05\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.9436\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.2698\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2040\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2.1\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9677\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e4.5939\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1821\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.26\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.20\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(2.0%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1283934\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e25261\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e278524\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e5480\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e14000\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e280\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\u0026nbsp;\u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eFMB-19-12\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.9435\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.2699\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2041\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1.7\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9702\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.6165\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1789\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e19.79\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.37\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(1.9%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2440545\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e45594\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e229294\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e4284\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e11590\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e220\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eF5a\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eFMB-18-04\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.9429\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.2697\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2044\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1.8\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9709\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e42.9287\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1789\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e79.07\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1.68\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(2.1%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e9716105\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e205863\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e226122\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e4791\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e11460\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e240\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\u0026nbsp;\u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eFMB-18-08\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.9438\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.2688\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2043\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2.0\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9675\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e25.5955\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1787\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e48.96\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.91\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(1.9%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e6008892\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e111455\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e234413\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e4348\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e11920\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e220\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\u0026nbsp;\u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eFMB-18-09\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.9438\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.2689\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2042\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2.1\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9703\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e23.8501\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1790\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e34.29\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.64\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(1.9%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e4215324\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e79209\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e176366\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e3314\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e9100\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e170\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\u0026nbsp;\u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eFMB-19-13\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.9432\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.2694\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2044\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1.6\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9728\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.5569\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1758\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e18.60\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.35\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(1.9%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2254712\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e42127\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e212986\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e3979\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10760\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e200\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJ7\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJAM-18-11\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.8904\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.1871\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2520\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1.3\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9634\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e9.2555\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1806\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e30.46\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.56\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(1.9%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e3778652\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e70081\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e407782\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e7563\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e14710\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e270\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\u0026nbsp;\u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJAM-19-19\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.8904\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.1875\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2522\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2.0\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9607\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.6142\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1798\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e34.00\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.64\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(1.9%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e4214518\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e78808\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e396476\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e7414\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e14420\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e270\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\u0026nbsp;\u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJAM-20-23\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.8904\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.1872\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2521\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2.9\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9620\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e11.3598\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1807\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e35.08\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.71\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(2.0%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e4383259\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e88749\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e385607\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e7807\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e14130\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e290\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJ6\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJAM-18-13\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.8901\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.1838\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2432\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e3.4\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9781\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e16.5606\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1806\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e44.59\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.83\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(1.9%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e5532868\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e103026\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e333831\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e6216\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e12880\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e240\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\u0026nbsp;\u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJAM-19-20\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.8893\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.1865\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2445\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1.5\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9604\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.6338\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1801\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e26.96\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.50\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(1.9%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e3347499\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e62609\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e314211\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e5877\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e12120\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e230\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJ5\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJAM-20-24\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.8895\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.1829\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2380\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2.4\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9779\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e6.8428\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1805\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e15.93\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.30\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(1.9%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1987961\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e37023\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e290103\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e5403\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e11620\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e220\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\u0026nbsp;\u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJAM-20-25\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.8893\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.1835\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2389\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1.7\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9768\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.9885\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1798\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e26.46\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.52\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(2.0%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e3289758\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e64839\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e299123\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e5896\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e11830\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e230\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJ3-4\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJAM-20-26\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.8898\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.1740\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2065\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1.8\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9412\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e11.5032\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1796\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e18.81\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.40\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(2.1%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2335435\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e49824\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e202777\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e4326\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10490\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e220\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\u0026nbsp;\u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u003cstrong\u003eJAM-20-27\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e46.8908\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e10.1733\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2047\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e1.4\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.9499\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e11.5197\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.1803\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e20.97\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e0.39\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e(1.9%)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e2613912\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e48590\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e226661\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e4213\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e11650\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cp\u003e\u0026plusmn;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd align=\"char\"\u003e\n \u003cp\u003e220\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003c/tbody\u003e\n \u003c/table\u003e\n\u003c/div\u003e\n\u003cp\u003e\u003cbr\u003e\u003c/p\u003e\n\u003cp\u003eAt \u003cstrong\u003eJamtal\u003c/strong\u003e, our focus was on a steep (\u0026gt;30\u0026deg;) valley flank that features a right-lateral moraine set which was shaped by a former tributary glacier (Futsch\u0026ouml;l glacier; Figures \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003ea-b, S2, and S3). The uppermost landform selected for \u003csup\u003e10\u003c/sup\u003eBe surface exposure dating is \u003cstrong\u003eJ7\u003c/strong\u003e at an elevation of ca. 2520 m a.s.l. (Figure \u003cspan class=\"InternalRef\"\u003e4\u003c/span\u003ea). The three sampled boulders rest on a till-covered lineament and yield a landform age of \u003cstrong\u003e14.4 \u0026plusmn; 1.0 ka (Figure S1a)\u003c/strong\u003e. Around 80 m lower, at ca. 2440 m a.s.l., a sharp-crested moraine (\u003cstrong\u003eJ6\u003c/strong\u003e) was deposited that consists mainly of fine sediments (Figure \u003cspan class=\"InternalRef\"\u003e4\u003c/span\u003eb) and features two boulders that qualified for sampling. Corresponding ages are 12.9 \u0026plusmn; 0.2 ka and 12.1 \u0026plusmn; 0.2 ka. The ice margin geomorphology another level below denoted as \u003cstrong\u003eJ5\u003c/strong\u003e (Figure \u003cspan class=\"InternalRef\"\u003e4\u003c/span\u003ed), differs from J6 in the absence of a distinct ridge and in the abundance of boulders of which two were selected for dating and yield ages of 11.6 \u0026plusmn; 0.2 ka and 11.8 \u0026plusmn; 0.2 ka. Two boulders in the main valley embedded in lateral and in terminal moraines (\u003cstrong\u003eJ3\u0026ndash;4\u003c/strong\u003e, Figure \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003ec-d) give ages of 10.4 \u0026plusmn; 0.2 ka and 11.6 \u0026plusmn; 0.2 ka and extend the Holocene moraine chronology published for the valley by Braumann, et al. \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e9\u003c/span\u003e\u003c/sup\u003e.\u003c/p\u003e\n\u003cp\u003eAt \u003cstrong\u003eFimbatal\u003c/strong\u003e, samples were collected from two adjacent latero-frontal moraine ridges (\u003cstrong\u003eF5a\u003c/strong\u003e and \u003cstrong\u003eF5b\u003c/strong\u003e) deposited at an elevation of ca. 2040 m a.s.l. (Figure \u003cspan class=\"InternalRef\"\u003e5\u003c/span\u003e). The outer ridge (\u003cstrong\u003eF5b\u003c/strong\u003e) consists of mostly fine sediments and is overgrown by vegetation. It is preserved only on the east side of the creek and has few boulders exposed, two of which were sampled and yield ages of 14.0 \u0026plusmn; 0.3 ka (FMB-18-05) and 11.6 \u0026plusmn; 0.2 ka (FMB-19-12). Although FMB-18-05 agrees within errors with boulder ages along J7 at Jamtal, we reject the age as an outlier due to its stratigraphic position. A terminal moraine at Fimbatal, which is equivalent to the lateral ice-margin position at Jamtal, should be positioned further downstream. FMB-18-05 probably overestimates the age of F5b, most likely due to inheritance from one or multiple earlier exposure events.\u003c/p\u003e\n\u003cp\u003eThe inner ridge (\u003cstrong\u003eF5a\u003c/strong\u003e) is preserved on both sides of the creek and exhibits a blocky structure in its frontal section caused by the outwash of fine-grained material. Exposure ages of the four boulders along F5a range between 11.9 \u0026plusmn; 0.2 ka and 9.1 \u0026plusmn; 0.2 ka. The age of FMB-18-09 (9.1 \u0026plusmn; 0.2 ka) falls within a period during the Holocene when most glaciers had probably retreated inboard the subsequent LIA ice margin \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e15\u003c/span\u003e\u0026ndash;\u003cspan class=\"CitationRef\"\u003e17\u003c/span\u003e\u003c/sup\u003e. For reference, the LIA terminal moraine in this valley is located at an elevation of ca. 2520 m a.sl., i.e. around 500 m higher and almost 7 km upstream of F5a/b (Figure \u003cspan class=\"InternalRef\"\u003e1\u003c/span\u003eb). These vertical and lateral distances cannot be reconciled with the age and location of FMB-18-09. Therefore, we discard the age for our interpretation. Ages of the remaining moraine boulders featured by F5a in concert with the age of FMB-19-12 of F5b correlate with the moraine age of J5 at Jamtal. The Fimbatal geochronology hence makes a case for two closely spaced stable ice margins toward the end of the YD.\u003c/p\u003e"},{"header":"3 Discussion","content":"\u003cp\u003eBoulder ages in both valleys fall into three periods: \u003cstrong\u003e(1)\u003c/strong\u003e the Oldest Dryas to B\u0026oslash;lling (J7), \u003cstrong\u003e(2)\u003c/strong\u003e the Younger Dryas (J6, J5, F5a, and F5b), and \u003cstrong\u003e(3)\u003c/strong\u003e the early Holocene (J3\u0026ndash;4), and are discussed in this order.\u003c/p\u003e\n\u003cp\u003ePre-B\u0026oslash;lling to B\u0026oslash;lling transition\u003c/p\u003e\n\u003cp\u003eThe deposition of J7 (14.4 \u0026plusmn; 1.0 ka) occurred during a period when regional climate was transitioning from stadial to interstadial conditions, i.e., from the Oldest Dryas cold phase to the B\u0026oslash;lling warm phase. We review deglaciation of the European Alps in the millennia before the deposition of J7 to place the new moraine records at Jamtal and Fimbatal in a coherent temporal and spatial context of the Alpine LG.\u003c/p\u003e\n\u003cp\u003eDuring the Gschnitz stadial, a well-documented post-LGM glacier readvance around 17\u0026ndash;16 ka, the uppermost sections of the Alpine main valleys and their tributary valleys were glaciated \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e18\u003c/span\u003e\u003c/sup\u003e. This phase of readvance that is often associated with Heinrich event 1 in the North Atlantic \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e19\u003c/span\u003e\u003c/sup\u003e was followed by a period of still relatively low mean annual temperatures, but slightly increasing summer temperatures paralleling increasing solar insolation (Figures \u003cspan class=\"InternalRef\"\u003e6\u003c/span\u003ea and \u003cspan class=\"InternalRef\"\u003e6\u003c/span\u003ee). Despite the probably cold winters, glaciers in the Alps responded to the warmer summers after 16 ka \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e20\u003c/span\u003e\u003c/sup\u003e and retreated to higher elevations. Several recent studies have investigated the pace of post-LGM deglaciation in selected inner-alpine pass regions by applying surface exposure dating to bedrock sections along transects \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e21\u003c/span\u003e\u0026ndash;\u003cspan class=\"CitationRef\"\u003e27\u003c/span\u003e\u003c/sup\u003e. Results indicate that major ice transfluence zones, for instance, the Gotthard, the Grimsel, and the Simplon passes became ice-free between ca. 16 and 14 ka. However, local glaciers with extents that exceeded the subsequent YD glaciation may have been present until the B\u0026oslash;lling. At Jamtal, the deposition of a moraine outboard the Egesen moraines around 14.4 \u0026plusmn; 1.0 ka confirms the timing of ice decay reconstructed in these deglaciation studies and indicates that glacier retreat between ca. 16 ka and ca. 14 ka was discontinuous.\u003c/p\u003e\n\u003cp\u003eSince LG moraines provide geomorphological evidence of discontinuous deglaciation, their identification in alpine valleys allows inferences about cold phases that interrupted the general post-LGM warming trend. The relative moraine stratigraphy of the Alpine region is based on this approach and suggests up to six more or less recognized stadials \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e28\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e29\u003c/span\u003e\u003c/sup\u003e, most prominently the above described \u0026lsquo;Gschnitz\u0026rsquo; stadial, and the subsequent, upstream \u0026lsquo;Egesen\u0026rsquo; stadial. Egesen moraines are distinct multi-ridge structures ubiquitous in high-Alpine valleys and are accepted as the morphostratigraphical equivalent of YD cooling \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e7\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e30\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e31\u003c/span\u003e\u003c/sup\u003e. A less conspicuous stadial, proposed as a stable ice margin in between the Gschnitz and the Egesen moraines, is the putative \u0026lsquo;Daun\u0026rsquo; stadial. Daun moraines are described as recessional moraines, with less pronounced crests, often with few boulders, and sometimes affected by solifluction. They are assumed to indicate pre-B\u0026oslash;lling glaciers that are limited to local, inner-alpine locations, being closer to the subsequent Egesen moraines than to Gschnitz. The presence of corresponding moraines in the Alps is sparse, therefore its acknowledgment as an independent stadial that is discernable at several sites across the Alps remains controversial \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e32\u003c/span\u003e\u003c/sup\u003e. The underrepresentation of presumable Daun moraines in geochronological studies in the Alps may be owed to their unspectacular morphology in tandem with poorer preservation, and fewer datable boulders. Nevertheless, the morphology and age of several landforms in the Alps, including the J7 moraine at Jamtal, resemble the characteristics of the Daun stadial. In a geochronological study at the Great Aletsch glacier, Schindelwig, et al. \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e10\u003c/span\u003e\u003c/sup\u003e investigated an ice margin indicative of glacier extents that exceed the Egesen extent. They obtained a (recalculated) age of 14.4 \u0026plusmn; 0.7 ka (their sample VBA-7) for a boulder sitting on top of a bedrock section that deglaciated at the same time. The authors interpret the site as an LG ice margin of the Great Aletsch glacier. B\u0026ouml;hlert, et al. \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e26\u003c/span\u003e\u003c/sup\u003e yielded a (recalculated) age of 15.2 \u0026plusmn; 1.9 ka for a boulder (their sample VM7) embedded in a lateral moraine outboard the presumable Egesen moraine at Val Mulix (Switzerland) and ascribed the landform to the Daun stadial. Rolland, et al. \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e27\u003c/span\u003e\u003c/sup\u003e combined the analysis of proglacial lake sediments in the Argentera-Mercantour Massif with exposure dating of glacial features in the region and identified an LG moraine that was deposited ca. 14.6 \u0026plusmn; 0.9 ka (Vens moraine, n = 3). These dated boulders and landforms, albeit limited in number, are in good agreement with the age of J7 and suggest moraine formation between ca. 16 and 14 ka in the Alps. However, any attempt to correlate J7 with the traditional Daun stadial first requires the geomorphological evaluation and dating of the type locality in the Austrian Stubai Alps \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e33\u003c/span\u003e\u003c/sup\u003e.\u003c/p\u003e\n\u003cp\u003eConsidering the age range of J7 (14.4 \u0026plusmn;1.0), the landform could also have been deposited at the onset of the B\u0026oslash;lling interstadial, during the Older Dryas cold snap (ca. 14 ka), or even during the subsequent Aller\u0026oslash;d interstadial (until 12.9 ka). The B-A interstadial was identified in numerous climate archives in the Northern Hemisphere \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e34\u003c/span\u003e\u0026ndash;\u003cspan class=\"CitationRef\"\u003e38\u003c/span\u003e\u003c/sup\u003e. Its onset around 14.6 ka is characterized by an abrupt temperature increase that induced substantial changes in environmental and vegetational conditions \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e39\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e40\u003c/span\u003e\u003c/sup\u003e. Summer temperatures increased by several degrees in the Alps \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e35\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e37\u003c/span\u003e\u003c/sup\u003e, transitioning from cooler stadial to warmer interstadial levels (Figure \u003cspan class=\"InternalRef\"\u003e6\u003c/span\u003ec-d). Glaciers responded to this warming and might have retreated to the highest cirques of the Alps or disappeared completely during the B-A temperature plateau. The demise of glaciers during this interstadial appears in conflict with concurrent moraine formation of the J7 moraine outboard the subsequent Egesen ice margin. Yet, weakening of the Atlantic Meridional Overturning Circulation (AMOC) may explain centennial-scale cooling during general warming and contemporaneous stabilization or readvance of glaciers in the European Alps. Freshwater input into the North Atlantic Ocean during the deglaciation of adjacent ice sheets has the potential to decelerate or even shut down the warm northwards flowing AMOC limb and to temporarily reduce heat transport to Northern Europe \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e41\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e42\u003c/span\u003e\u003c/sup\u003e. Evidence of repeated freshening of ocean water between 15.8 and 12.6 ka has for instance been detected in a sediment core south of Iceland and has been linked to the deglaciation of the Laurentide ice sheet \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e43\u003c/span\u003e\u003c/sup\u003e. A reduction of poleward heat transport may have led to centennial-scale episodes of cooling detected in Northern and Central Europe, such as the Older Dryas and the later Gerzensee oscillations (13.3-13.0 ka) \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e39\u003c/span\u003e\u003c/sup\u003e. The link between the deglaciation of the Laurentide ice sheet, resulting in freshwater input into the North Atlantic, and cooling in Europe has been suggested as an explanation for abrupt centennial-scale cooling in the context of the YD-Holocene transition \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e44\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e45\u003c/span\u003e\u003c/sup\u003e. Moraine formation as a result of this teleconnection during the YD-Holocene transition has recently been proposed by Young, et al. \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e46\u003c/span\u003e\u003c/sup\u003e for the Greenland ice sheet, by Protin, et al. \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e8\u003c/span\u003e\u003c/sup\u003e for mountain glaciers in the French Alps, and by Braumann, et al. \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e9\u003c/span\u003e\u003c/sup\u003e for the Austrian Alps. Comparing the warming during the pre-B\u0026oslash;lling to B\u0026oslash;lling transition and during the YD-Holocene transition (Figure \u003cspan class=\"InternalRef\"\u003e6\u003c/span\u003ee), we tentatively suggest brief episodes of an AMOC weakening and subsequent cooling in Europe. Even though the causation between B\u0026oslash;lling warming, freshwater input into the Atlantic, and the AMOC circulation is elusive, we note that the timing of B\u0026oslash;lling warming parallels MWP1A, a sea-level rise of about 12\u0026ndash;22 m within a few centuries (Figure \u003cspan class=\"InternalRef\"\u003e6\u003c/span\u003eb) \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e47\u003c/span\u003e\u003c/sup\u003e. The source of MWP1A remains under debate and has often been attributed to the Antarctic ice sheet alone \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e48\u003c/span\u003e\u003c/sup\u003e. However, recent sea-level fingerprinting and ice sheet modeling studies suggest that the melting of ice sheets in the Northern Hemisphere likely has contributed to massive sea-level rise at that time and may have caused centennial-scale cold lapses \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e49\u003c/span\u003e\u0026ndash;\u003cspan class=\"CitationRef\"\u003e51\u003c/span\u003e\u003c/sup\u003e.\u003c/p\u003e\n\u003cp\u003eBoth scenarios \u0026ndash; moraine deposition prior to or during the B\u0026oslash;lling \u0026ndash; are plausible, but more direct age data covering that period are needed to better constrain moraine deposition and thus cooling between 16\u0026ndash;14 ka in the European Alps. Interestingly, when comparing the (pre-)B\u0026oslash;lling moraine age of J7 with mountain glacier records beyond the Alps, we find similar intervals of moraine formation in Norway \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e52\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e53\u003c/span\u003e\u003c/sup\u003e, in Patagonia \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e54\u003c/span\u003e\u0026ndash;\u003cspan class=\"CitationRef\"\u003e58\u003c/span\u003e\u003c/sup\u003e and New Zealand \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e59\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e60\u003c/span\u003e\u003c/sup\u003e, and the Himalaya region \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e61\u003c/span\u003e\u003c/sup\u003e. In the Southern Hemisphere, the climatic explanation for this phase of glacier advance is the Antarctic Cold Reversal (ACR; 14.5-12.7 ka), a millennial-scale cold phase documented in Antarctic ice cores \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e62\u003c/span\u003e\u003c/sup\u003e. The extent to which this cold phase propagated from Antarctica and the Southern Hemisphere further to the North remains controversial but we note that moraine formation indicated by J7 falls within the early phase of the ACR.\u003c/p\u003e\n\u003cp\u003eYounger Dryas \u0026ndash; Egesen moraines\u003c/p\u003e\n\u003cp\u003eThe next LG time slice that is captured by the new moraine chronologies of both valleys is the YD period. We interpret moraines J6 and J5 at Jamtal and F5a and F5b at Fimbatal as Egesen moraines that portray the fine structure of ice retreat during this final stadial before Holocene warming (Figure \u003cspan class=\"InternalRef\"\u003e6\u003c/span\u003ee). J6 at Jamtal indicates an ice margin in the early phase of the YD. The lower J5 moraine and F5a/b at Fimbatal delimit glacier extents toward the very end of the YD. Exposure ages from these landforms confirm relative age estimates from a previous study in the Silvretta region that focused on geomorphology and stratigraphy \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e63\u003c/span\u003e\u003c/sup\u003e.\u003c/p\u003e\n\u003cp\u003eThe Egesen moraine sequence at Jamtal shows that the ice surface lowered by about 55 m from J6 (ca. 2440 m a.s.l.) to J5 (2385 m a.sl.) within a few centuries (Figure \u003cspan class=\"InternalRef\"\u003e4\u003c/span\u003ec), hence supporting the hypothesis that climate conditions became gradually milder through the YD \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e64\u003c/span\u003e\u003c/sup\u003e. Glacier retreat with intermittent phases of glacier stabilization through the YD is observed at different places of the Northern Hemisphere \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e7\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e52\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e65\u003c/span\u003e\u003c/sup\u003e and coincides with slightly increasing summer temperatures (Figure \u003cspan class=\"InternalRef\"\u003e6\u003c/span\u003ee) \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e34\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e35\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e66\u003c/span\u003e\u003c/sup\u003e. The mountain glacier record of the Southern Hemisphere indicates moraine deposition through glacier retreat during the same time interval \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e57\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e67\u003c/span\u003e\u003c/sup\u003e, which corroborates the gradual expansion of YD cooling towards the Southern Hemisphere \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e68\u003c/span\u003e\u003c/sup\u003e.\u003c/p\u003e\n\u003cp\u003eEarly Holocene\u003c/p\u003e\n\u003cp\u003eIce-surface lowering during the YD from J6 to J5 was rapid but the rate of glacier change during the transition from the YD to the EH was even faster. The downwasting of Jamtal glacier and its tributary Futsch\u0026ouml;l glacier during this period is best illustrated by comparing moraine segments J5 and to J3\u0026ndash;4 (Figure \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003e). Even though the boulder ages of J5 and JAM-20-27 (J3\u0026ndash;4) are statistically indistinguishable, the associated landforms indicate very different glacier positions (\u003cstrong\u003eFigure 7a-b\u003c/strong\u003e). J5 marks the right-lateral ice margin of the tributary (Futsch\u0026ouml;l) glacier when it still converged with the main (Jamtal) glacier. In turn, J3\u0026ndash;4 indicates much smaller glacier extents when the main and the tributary glaciers were separated, which implies deglaciation of the valley flank within a few centuries (Figure \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003ea, S2). The new early Holocene terminus of Jamtal glacier marked by JAM-20-27 (Figure \u003cspan class=\"InternalRef\"\u003e3\u003c/span\u003ed) is located only around 900 m outboard the Holocene/LIA moraine (\u003cstrong\u003eFigure 7c\u003c/strong\u003e). J3\u0026ndash;4 is interpreted as the equivalent of the right lateral early Holocene moraine set (JR3\u0026ndash;4) that was mapped and dated in a previous study \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e9\u003c/span\u003e\u003c/sup\u003e, which in concert with the adjacent EH Laraintal chronology indicates moraine deposition and thus glacier stabilization ca. 11.0 \u0026plusmn; 0.7 ka (Figures \u003cspan class=\"InternalRef\"\u003e6\u003c/span\u003ef, 7b, and S1). The timing of moraine formation overlaps with the Preboreal Oscillation, a centennial-scale cold pulse in (Northern) Europe which was likely caused by AMOC weakening due to freshwater input into the Atlantic \u0026ndash; the same mechanism that was tentatively proposed earlier for the deposition of J7 during the early B\u0026oslash;lling (\u003cstrong\u003esection 3.1\u003c/strong\u003e). Similar to the (pre-)B\u0026oslash;lling and YD period, the synchronicity of mountain glacier stabilization during the EH is observed in glaciated regions of both hemispheres \u003csup\u003e46,69\u0026minus;72\u003c/sup\u003e.\u003c/p\u003e\n\u003cp\u003eSilvretta glaciers probably remained outboard their subsequent LIA ice margins for the next several centuries but retreated to LIA-like configurations around 10 ka, which is shown based on a \u003csup\u003e10\u003c/sup\u003eBe moraine chronology from the adjacent Ochsental (\u003cstrong\u003eFigure 7c\u003c/strong\u003e) \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e17\u003c/span\u003e\u003c/sup\u003e. Throughout the rest of the Holocene, they oscillated inboard the 10 ka limits (e.g., \u003cstrong\u003eFigure 7d\u003c/strong\u003e) with advances(s) to this position possibly during the Neoglacial and certainly during the LIA \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e73\u003c/span\u003e\u003c/sup\u003e.\u003c/p\u003e\n\u003cp\u003eBroader relevance of the new moraine chronologies\u003c/p\u003e\n\u003cp\u003eThe \u003csup\u003e10\u003c/sup\u003eBe datasets from the Silvretta Massif are to date the most detailed cosmogenic-nuclide-based mountain glacier records in the Eastern European Alps. They pinpoint the timing of moraine formation in the region around 14.4 \u0026plusmn; 1.0 ka, during the YD between 12.9 and 11.7 ka, and during the Early Holocene around 11.0 \u0026plusmn; 0.7 ka \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e9\u003c/span\u003e\u003c/sup\u003e and around 9.9 \u0026plusmn; 0.7 ka \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e17\u003c/span\u003e\u003c/sup\u003e. They allow for robust glacier reconstructions at different times during the LG and the Holocene, contribute to our understanding of the climate transitioning from glacial to interglacial conditions, and provide valuable constraints for the modeling of paleoglaciers.\u003c/p\u003e\n\u003cp\u003eA comparison of the mountain glacier record on a global scale shows that glaciers in both hemispheres deposited moraines around 15\u0026ndash;14 ka, during the YD, and during the EH. The next step is to investigate whether these similarities are coincidental, or due to large-scale climatic forcing.\u003c/p\u003e\n\u003cp\u003eThe reconstruction of Silvretta glaciers during recent geological periods shows their sensitive response to natural warming and places the magnitude and impact of anthropogenic climate change in a natural context.\u003c/p\u003e"},{"header":"Methods","content":"\u003cp\u003eGeomorphological mapping\u003cbr\u003eHertl \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e63\u003c/span\u003e\u003c/sup\u003e, and references therein developed a relative moraine stratigraphy for the region on which this work is based. The pre-existing geomorphological maps were updated and supplemented with information gained during several field campaigns in the summers of 2018 to 2021, from remote sensing data \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e74\u003c/span\u003e,\u003cspan class=\"CitationRef\"\u003e75\u003c/span\u003e\u003c/sup\u003e and drone imagery. Glacier reconstructions of Jamtal glacier for the Holocene including corresponding maps are presented in Braumann, et al. \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e9\u003c/span\u003e\u003c/sup\u003e. With this study, we extend the Jamtal glacier chronology into the LG and focus on landforms that evidence glacier oscillations during that period by mapping and dating margins outboard the Holocene moraines. Reconstructions of paleoglaciers are complemented with glaciological data of modern, annual- to decadal-scale glaciological data including observations of glacier mass balances, front variation, and ice-covered area \u003csup\u003e14,76\u0026minus;78\u003c/sup\u003e.\u003c/p\u003e\n\u003cp\u003eSurface exposure dating with \u003csup\u003e10\u003c/sup\u003eBe\u003c/p\u003e\n\u003cp\u003eWhen fresh quartz-containing rock surfaces are exposed to cosmic radiation, the production of the cosmogenic radionuclide \u003csup\u003e10\u003c/sup\u003eBe begins according to the nuclide-specific production rate (ca. 4 atoms \u003csup\u003e\u0026minus;g \u0026minus;yr\u003c/sup\u003e). The longer a surface has been exposed, the more \u003csup\u003e10\u003c/sup\u003eBe accumulates \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e79\u003c/span\u003e\u003c/sup\u003e. Thus, the nuclide content in rock surfaces is a function of exposure time. This principle is used in the application of surface exposure dating to glacial landforms. A moraine boulder that is sampled for \u003csup\u003e10\u003c/sup\u003eBe analysis has ideally been eroded from bedrock beneath the glacier, has then been transported sub- or englacially, and has finally been deposited on a moraine crest that marks a stable ice margin. It has therefore not been exposed to cosmic radiation before its deposition on the moraine so that its radionuclide inventory is \u0026lsquo;zeroed\u0026rsquo;. If these assumptions are true, the \u003csup\u003e10\u003c/sup\u003eBe inventory measured in a rock surface after exposure will produce an age that reflects the boulder\u0026rsquo;s melt out of glacial ice, or in other words, the onset of ice retreat, hence warming.\u003c/p\u003e\n\u003cp\u003eRock samples were collected using an electric saw and hammer and chisel. The sample location was measured using a hand-held GPS device. Strike and dip angles of sampled rock surfaces were quantified using a geological compass. Samples were preferably collected from boulder tops at windswept locations to minimize shielding effects due to snow and/or sediment cover. We avoided surfaces that were affected by exfoliation and prioritized boulder locations with striations preserved on the surface, which is indicative of low postglacial erosion. For more details on our sample selection criteria, we refer to Braumann, et al. \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e17\u003c/span\u003e\u003c/sup\u003e\u0026rsquo;s supplement, their Table S1.\u003c/p\u003e\n\u003cp\u003eMechanical sample preparation was accomplished at the Department of Lithospheric Research of the University of Vienna and at the Lamont-Doherty Earth Observatory (LDEO). Whole-rock samples were crushed to grain sizes between 63 and 500 \u0026micro;g using a mill or a jaw crusher. Mineral separation strategies included magnetic separation, boiling with phosphoric acid, froth flotation, density separation and repeated (\u0026gt;3) leaches with hydrofluoric acid and nitric acid at concentrations between 1% and 5% \u003csup\u003e80\u003c/sup\u003e. Purified quartz yields, the target mineral for \u003csup\u003e10\u003c/sup\u003eBe extraction, ranged from 1.1\u0026ndash;11.3% (\u003cstrong\u003eTable S1\u003c/strong\u003e). Samples were processed in four batches (\u003cstrong\u003eTable S2\u003c/strong\u003e) with quartz weights ranging from 4.5939 g to 42.9287 g (Table \u003cspan class=\"InternalRef\"\u003e1\u003c/span\u003e). All samples were spiked with the LDEO \u003csup\u003e9\u003c/sup\u003eBe carrier (#7) made of deep-mine beryl which has a concentration of approximately 1000 ppm. The extraction of \u003csup\u003e10\u003c/sup\u003eBe was accomplished following the LDEO protocol described in LDEO \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e81\u003c/span\u003e\u003c/sup\u003e. Isotope ratios in samples (\u003csup\u003e10\u003c/sup\u003eBe/\u003csup\u003e9\u003c/sup\u003eBe) were measured at the Center for Accelerator Mass Spectrometry (CAMS) facility, Lawrence Livermore National Laboratory (LLNL) using the 07KNDSTD3110 standard with a \u003csup\u003e10\u003c/sup\u003eBe/\u003csup\u003e9\u003c/sup\u003eBe ratio of 2.85 x 10\u003csup\u003e\u0026minus;12 82\u003c/sup\u003e.\u003c/p\u003e\n\u003cp\u003eExposure age calculations including statistical outlier identification (\u0026Chi;\u003csup\u003e\u003cspan class=\"CitationRef\"\u003e2\u003c/span\u003e\u003c/sup\u003e test) were performed using the online calculator formerly known as the CRONUS-Earth online calculator v3 \u003csup\u003e83\u003c/sup\u003e. We used the local \u0026lsquo;Swiss\u0026rsquo; production rate \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e84\u003c/span\u003e\u003c/sup\u003e and chose the time-dependent \u0026lsquo;Lm\u0026rsquo; scaling scheme \u003csup\u003e\u003cspan class=\"CitationRef\"\u003e85\u003c/span\u003e\u003c/sup\u003e. In the data presentation and discussion, we distinguish between exposure ages of individual boulders and moraine ages. Boulder ages are reported with 1\u0026sigma; analytical uncertainties and a 1 % error on the carrier concentration, but without uncertainties on the production rate as this source of uncertainty is constant for all boulders sampled from the same area. For moraine ages (n \u0026ge; 3), the production rate error is propagated in quadrature to analytical and carrier uncertainties to allow the correlation of robust landform ages with moraine records from other regions.\u003c/p\u003e"},{"header":"Declarations","content":"\u003ch2\u003eAcknowledgements\u003c/h2\u003e\n\u003cp\u003eThis study was sponsored by inatura Museum GmbH and is based upon work supported by the National Science Foundation under grant no. NSF-1853881. SMB is a recipient of a DOC Fellowship of the Austrian Academy of Sciences (OeAW) at the Institute of Applied Geology, University of Natural Resources and Life Sciences (BOKU) Vienna. For research visits at the Lamont-Doherty Earth Observatory (LDEO) of Columbia University, SMB received a Marietta Blau scholarship sponsored by OeAD GmbH, a Marshall Plan scholarship provided by the Austrian Marshall Plan Foundation and financial support from BOKU\u0026rsquo;s \u0026lsquo;Transitions to Sustainability\u0026rsquo; (T2S) doctoral school. SMB thanks the LDEO cosmogenic nuclide laboratory staff Roseanne Schwartz and Jean Hanley for advice during sample processing and Alan J. Hidy at CAMS-LLNL for \u003csup\u003e10\u003c/sup\u003eBe sample analysis. SMB is grateful to Dominik Blasenbauer for assistance in the field, and to Allie Balter-Kennedy for helpful discussions on the topic of this manuscript.\u003c/p\u003e\n\u003ch2\u003eAuthor Contribution\u003c/h2\u003e\n\u003cp\u003eSMB and JMS designed the study. All authors carried out field work. SMB accomplished cosmogenic nuclide sample preparation and age calculation. SMB wrote the manuscript and prepared the figures. All authors made substantial contributions to the data interpretation and revised and edited the manuscript.\u003c/p\u003e\n\u003ch2\u003eData availability\u003c/h2\u003e\n\u003cp\u003eAll analytical information associated with cosmogenic nuclide measurements is listed in the tables in the Supplement and will be made available via the ICE-D Alpine database (\u003ca href=\"http://alpine.ice-d.org/\"\u003ehttp://alpine.ice-d.org/\u003c/a\u003e).\u003c/p\u003e"},{"header":"References","content":"\u003cp\u003e1 Huston, A., Siler, N., Roe, G. H., Pettit, E. \u0026amp; Steiger, N. J. Understanding drivers of glacier-length variability over the last millennium. The Cryosphere \u003cstrong\u003e15\u003c/strong\u003e, 1645-1662, doi:10.5194/tc-15-1645-2021 (2021).\u003c/p\u003e\n\u003cp\u003e2 Oerlemans, J. Extracting a climate signal from 169 glacier records. Science \u003cstrong\u003e308\u003c/strong\u003e, 675-677 (2005).\u003c/p\u003e\n\u003cp\u003e3 IPCC. Climate Change 2021: The Physical Science Basis. Contribution of Working Group I to the Sixth Assessment Report of the Intergovernmental Panel on Climate Change. (2021).\u003c/p\u003e\n\u003cp\u003e4 Hock, R. et al. in IPCC Special Report on the Ocean and Cryosphere in a Changing Climate (eds H.-O. Pörtner et al.) 131-202 (IPCC - Intergovernmental Panel on Climate Change, 2019).\u003c/p\u003e\n\u003cp\u003e5 Salcher, B., Prasicek, G., Baumann, S. \u0026amp; Kober, F. Alpine relief limited by glacial occupation time. Geology \u003cstrong\u003e49\u003c/strong\u003e, 1209-1213, doi:10.1130/G48639.1 (2021).\u003c/p\u003e\n\u003cp\u003e6 Cunningham, M. T., Stark, C. P., Kaplan, M. R. \u0026amp; Schaefer, J. M. Glacial limitation of tropical mountain height. Earth Surf Dynam \u003cstrong\u003e7\u003c/strong\u003e, 147-169, doi:10.5194/esurf-7-147-2019 (2019).\u003c/p\u003e\n\u003cp\u003e7 Ivy-Ochs, S. Glacier Variations in the European Alps at the End of the Last Glaciation. Cuad Investig Geogr \u003cstrong\u003e41\u003c/strong\u003e, 295-315, doi:10.18172/cig.2750 (2015).\u003c/p\u003e\n\u003cp\u003e8 Protin, M. et al. Millennial‐scale deglaciation across the European Alps at the transition between the Younger Dryas and the Early Holocene \u0026ndash; evidence from a new cosmogenic nuclide chronology. Boreas \u003cstrong\u003e50\u003c/strong\u003e, 671\u0026ndash;685, doi:10.1111/bor.12519 (2021).\u003c/p\u003e\n\u003cp\u003e9 Braumann, S. M. et al. Early Holocene cold snaps and their expression in the moraine record of the eastern European Alps. Clim. Past \u003cstrong\u003e17\u003c/strong\u003e, 2451-2479, doi:10.5194/cp-17-2451-2021 (2021).\u003c/p\u003e\n\u003cp\u003e10 Schindelwig, I., Akcar, N., Kubik, P. W. \u0026amp; Schl\u0026uuml;chter, C. Lateglacial and early Holocene dynamics of adjacent valley glaciers in the Western Swiss Alps. J Quaternary Sci \u003cstrong\u003e27\u003c/strong\u003e, 114-124, doi:10.1002/jqs.1523 (2012).\u003c/p\u003e\n\u003cp\u003e11 Schimmelpfennig, I. et al. Holocene glacier culminations in the Western Alps and their hemispheric relevance. Geology \u003cstrong\u003e40\u003c/strong\u003e, 891-894, doi:10.1130/G33169.1 (2012).\u003c/p\u003e\n\u003cp\u003e12 Friebe, G. Geologie der \u0026ouml;sterreichischen Bundesl\u0026auml;nder - Vorarlberg. 174 (Verlag der Geologischen Bundesanstalt, 2007).\u003c/p\u003e\n\u003cp\u003e13 Fuchs, G. \u0026amp; Oberhauser, R. 170 Galt\u0026uuml;r. (1990).\u003c/p\u003e\n\u003cp\u003e14 Fischer, A., Schwaizer, G., Seiser, B., Helfricht, K. \u0026amp; Stocker-Waldhuber, M. High-resolution inventory to capture glacier disintegration in the Austrian Silvretta. Cryosphere \u003cstrong\u003e15\u003c/strong\u003e, 4637-4654 (2021).\u003c/p\u003e\n\u003cp\u003e15 Nicolussi, K. \u0026amp; Patzelt, G. Discovery of early-Holocene wood and peat on the forefield of the Pasterze Glacier, Eastern Alps, Austria. Holocene \u003cstrong\u003e10\u003c/strong\u003e, 191-199, doi:10.1191/095968300666855842 (2000).\u003c/p\u003e\n\u003cp\u003e16 Patzelt, G. Das Bunte Moor in der Oberfernau (Stubaier Alpen, Tirol) \u0026ndash; Eine neu bearbeitete Schl\u0026uuml;sselstelle f\u0026uuml;r die Kenntnis der nacheiszeitlichen Gletscherschwankungen der Ostalpen. Jahrbuch der Geologischen Bundesanstalt \u003cstrong\u003eBand 156\u003c/strong\u003e, 97-107 (2016).\u003c/p\u003e\n\u003cp\u003e17 Braumann, S. M. et al. Holocene glacier change in the Silvretta Massif (Austrian Alps) constrained by a new Be-10 chronology, historical records and modern observations. Quaternary Sci Rev \u003cstrong\u003e245\u003c/strong\u003e, doi:10.1016/j.quascirev.2020.106493 (2020).\u003c/p\u003e\n\u003cp\u003e18 Ivy-Ochs, S., Kerschner, H., Kubik, P. W. \u0026amp; Schl\u0026uuml;chter, C. Glacier response in the European Alps to Heinrich Event 1 cooling: the Gschnitz stadial. J Quaternary Sci \u003cstrong\u003e21\u003c/strong\u003e, 115-130, doi:10.1002/jqs.955 (2006).\u003c/p\u003e\n\u003cp\u003e19 Heinrich, H. Origin and Consequences of Cyclic Ice Rafting in the Northeast Atlantic Ocean During the Past 130,000 Years. Quaternary Res \u003cstrong\u003e29\u003c/strong\u003e, 142-152, doi:10.1016/0033-5894(88)90057-9 (1988).\u003c/p\u003e\n\u003cp\u003e20 Schmidt, R., Weckstrom, K., Lauterbach, S., Tessadri, R. \u0026amp; Huber, K. North Atlantic climate impact on early late-glacial climate oscillations in the south-eastern Alps inferred from a multi-proxy lake sediment record. J Quaternary Sci \u003cstrong\u003e27\u003c/strong\u003e, 40-50, doi:10.1002/jqs.1505 (2012).\u003c/p\u003e\n\u003cp\u003e21 Dielforder, A. \u0026amp; Hetzel, R. The deglaciation history of the Simplon region (southern Swiss Alps) constrained by Be-10 exposure dating of ice-molded bedrock surfaces. Quaternary Sci Rev \u003cstrong\u003e84\u003c/strong\u003e, 26-38, doi:10.1016/j.quascirev.2013.11.008 (2014).\u003c/p\u003e\n\u003cp\u003e22 Hippe, K. et al. Chronology of Lateglacial ice flow reorganization and deglaciation in the Gotthard Pass area, Central Swiss Alps, based on cosmogenic Be-10 and in situ C-14. Quat Geochronol \u003cstrong\u003e19\u003c/strong\u003e, 14-26, doi:10.1016/j.quageo.2013.03.003 (2014).\u003c/p\u003e\n\u003cp\u003e23 Wirsig, C., Zasadni, J., Christl, M., Akcar, N. \u0026amp; Ivy-Ochs, S. Dating the onset of LGM ice surface lowering in the High Alps. Quaternary Sci Rev \u003cstrong\u003e143\u003c/strong\u003e, 37-50 (2016).\u003c/p\u003e\n\u003cp\u003e24 Kelly, M. A., Ivy-Ochs, S., Kubik, P. W., von Blanckenburg, F. \u0026amp; Schluchter, C. Chronology of deglaciation based on Be-10 dates of glacial erosional features in the Grimsel Pass region, central Swiss Alps. Boreas \u003cstrong\u003e35\u003c/strong\u003e, 634-643 (2006).\u003c/p\u003e\n\u003cp\u003e25 W\u0026ouml;lfler, A., Hampel, A., Dielforder, A., Hetzel, R. \u0026amp; Glotzbach, C. LGM ice extent and deglaciation history in the Gurktal and Lavantal Alps (eastern European Alps): first constraints from 10Be surface exposure dating of glacially polished quartz veins. J Quaternary Sci \u003cstrong\u003eOnline Version of Record before inclusion in an issue\u003c/strong\u003e, doi:10.1002/jqs.3399 (2021).\u003c/p\u003e\n\u003cp\u003e26 B\u0026ouml;hlert, R. et al. Application of a combination of dating techniques to reconstruct the Lateglacial and early Holocene landscape history of the Albula region (eastern Switzerland). Geomorphology \u003cstrong\u003e127\u003c/strong\u003e, 1-13 (2011).\u003c/p\u003e\n\u003cp\u003e27 Rolland, Y. et al. Deglaciation history at the Alpine-Mediterranean transition (Argentera-Mercantour, SW Alps) from Be-10 dating of moraines and glacially polished bedrock. Earth Surf Proc Land \u003cstrong\u003e45\u003c/strong\u003e, 393-410 (2020).\u003c/p\u003e\n\u003cp\u003e28 Maisch, M. Zur Gletscher- und Klimageschichte des alpinen Sp\u0026auml;tglazials. Geographica Helvetica \u003cstrong\u003e37\u003c/strong\u003e, 93-104, doi:10.5169/seals-58303 (1982).\u003c/p\u003e\n\u003cp\u003e29 Kerschner, H. in Klimawandel in \u0026Ouml;sterreich: Die letzten 20.000 Jahre ... und ein Blick voraus Vol. 6 alpine space \u0026ndash; man \u0026amp; environment (eds R. Schmidt, C. Matulla, \u0026amp; R. Psenner) 5-26 (Innsbruck University Press, 2009).\u003c/p\u003e\n\u003cp\u003e30 Federici, P. R. et al. Exposure age dating and Equilibrium Line Altitude reconstruction of an Egesen moraine in the Maritime Alps, Italy. Boreas \u003cstrong\u003e37\u003c/strong\u003e, 245-253, doi:10.1111/j.1502-3885.2007.00018.x (2008).\u003c/p\u003e\n\u003cp\u003e31 Kelly, M. A., Kubik, P. W., Von Blanckenburg, F. \u0026amp; Schl\u0026uuml;chter, C. Surface exposure dating of the Great Aletsch Glacier Egesen moraine system, western Swiss Alps, using the cosmogenic nuclide Be-10. J Quaternary Sci \u003cstrong\u003e19\u003c/strong\u003e, 431-441, doi:10.1002/jqs.854 (2004).\u003c/p\u003e\n\u003cp\u003e32 Reitner, J. M., Ivy-Ochs, S., Drescher-Schneider, R., Hajdas, I. \u0026amp; Linner, M. Reconsidering the current stratigraphy of the Alpine Lateglacial: Implications of the sedimentary and morphological record of the Lienz area (Tyrol/Austria). E\u0026amp;G Quaternary Sci. J. \u003cstrong\u003e65\u003c/strong\u003e, 113-144, doi:10.3285/eg.65.2.02 (2016).\u003c/p\u003e\n\u003cp\u003e33 Heuberger, H. Die Alpengletscher im Sp\u0026auml;t- und Postglazial. Eiszeitalter und Gegenwart \u003cstrong\u003e19\u003c/strong\u003e, 270-275 (1968).\u003c/p\u003e\n\u003cp\u003e34 Lauterbach, S. et al. Environmental responses to Lateglacial climatic fluctuations recorded in the sediments of pre-Alpine Lake Mondsee (northeastern Alps). J Quaternary Sci \u003cstrong\u003e26\u003c/strong\u003e, 253-267 (2011).\u003c/p\u003e\n\u003cp\u003e35 Heiri, O. et al. Palaeoclimate records 60-8 ka in the Austrian and Swiss Alps and their forelands. Quaternary Sci Rev \u003cstrong\u003e106\u003c/strong\u003e, 186-205, doi:10.1016/j.quascirev.2014.05.021 (2014).\u003c/p\u003e\n\u003cp\u003e36 Rasmussen, S. O. et al. A stratigraphic framework for abrupt climatic changes during the Last Glacial period based on three synchronized Greenland ice-core records: refining and extending the INTIMATE event stratigraphy. Quaternary Sci Rev \u003cstrong\u003e106\u003c/strong\u003e, 14-28, doi:10.1016/j.quascirev.2014.09.007 (2014).\u003c/p\u003e\n\u003cp\u003e37 Li, H. Y., Spotl, C. \u0026amp; Cheng, H. A high-resolution speleothem proxy record of the Late Glacial in the European Alps: extending the NALPS19 record until the beginning of the Holocene. J Quaternary Sci \u003cstrong\u003e36\u003c/strong\u003e, 29-39 (2021).\u003c/p\u003e\n\u003cp\u003e38 Kruger, S. \u0026amp; Damrath, M. In search of the Bolling-Oscillation: a new high resolution pollen record from the locus classicus Lake Bolling, Denmark. Veg Hist Archaeobot \u003cstrong\u003e29\u003c/strong\u003e, 189-211 (2020).\u003c/p\u003e\n\u003cp\u003e39 Ammann, B. et al. Vegetation responses to rapid warming and to minor climatic fluctuations during the Late-Glacial Interstadial (GI-1) at Gerzensee (Switzerland). Palaeogeogr Palaeocl \u003cstrong\u003e391\u003c/strong\u003e, 40-59, doi:10.1016/j.palaeo.2012.07.010 (2013).\u003c/p\u003e\n\u003cp\u003e40 Brisset, E. et al. Lateglacial/Holocene environmental changes in the Mediterranean Alps inferred from lacustrine sediments. Quaternary Sci Rev \u003cstrong\u003e110\u003c/strong\u003e, 49-71 (2015).\u003c/p\u003e\n\u003cp\u003e41 Broecker, W. S. The Great Ocean Conveyor. Oceanography \u003cstrong\u003e4\u003c/strong\u003e, 79-89, doi:10.5670/oceanog.1991.07 (1991).\u003c/p\u003e\n\u003cp\u003e42 McManus, J. F., Francois, R., Gherardi, J. M., Keigwin, L. D. \u0026amp; Brown-Leger, S. Collapse and rapid resumption of Atlantic meridional circulation linked to deglacial climate changes. Nature \u003cstrong\u003e428\u003c/strong\u003e, 834-837, doi:10.1038/nature02494 (2004).\u003c/p\u003e\n\u003cp\u003e43 Thornalley, D. J. R., McCave, I. N. \u0026amp; Elderfield, H. Freshwater input and abrupt deglacial climate change in the North Atlantic. Paleoceanography \u003cstrong\u003e25\u003c/strong\u003e, PA1201, doi:10.1029/2009PA001772 (2010).\u003c/p\u003e\n\u003cp\u003e44 Bjorck, S., Rundgren, M., Ingolfsson, O. \u0026amp; Funder, S. The Preboreal oscillation around the Nordic Seas: terrestrial and lacustrine responses. J Quaternary Sci \u003cstrong\u003e12\u003c/strong\u003e, 455-465 (1997).\u003c/p\u003e\n\u003cp\u003e45 Hald, M. \u0026amp; Hagen, S. Early preboreal cooling in the Nordic seas region triggered by meltwater. Geology \u003cstrong\u003e26\u003c/strong\u003e, 615-618 (1998).\u003c/p\u003e\n\u003cp\u003e46 Young, N. E. et al. Deglaciation of the Greenland and Laurentide ice sheets interrupted by glacier advance during abrupt coolings. Quaternary Sci Rev \u003cstrong\u003e229\u003c/strong\u003e, 106091, doi:10.1016/j.quascirev.2019.106091 (2020).\u003c/p\u003e\n\u003cp\u003e47 Lambeck, K., Rouby, H., Purcell, A., Sun, Y. Y. \u0026amp; Sambridge, M. Sea level and global ice volumes from the Last Glacial Maximum to the Holocene. P Natl Acad Sci USA \u003cstrong\u003e111\u003c/strong\u003e, 15296-15303, doi:10.1073/pnas.1411762111 (2014).\u003c/p\u003e\n\u003cp\u003e48 Mitrovica, J. X., Gomez, N. \u0026amp; Clark, P. U. The Sea-Level Fingerprint of West Antarctic Collapse. Science \u003cstrong\u003e323\u003c/strong\u003e, 753-753, doi:10.1126/science.1166510 (2009).\u003c/p\u003e\n\u003cp\u003e49 Lin, Y. et al. A reconciled solution of Meltwater Pulse 1A sources using sea-level fingerprinting. Nat Commun \u003cstrong\u003e12\u003c/strong\u003e, 2015, doi:10.1038/s41467-021-21990-y (2021).\u003c/p\u003e\n\u003cp\u003e50 Ivanovic, R. F., Gregoire, L. J., Wickert, A. D., Valdes, P. J. \u0026amp; Burke, A. Collapse of the North American ice saddle 14,500 years ago caused widespread cooling and reduced ocean overturning circulation. Geophys Res Lett \u003cstrong\u003e44\u003c/strong\u003e, 383-392, doi:10.1002/2016gl071849 (2017).\u003c/p\u003e\n\u003cp\u003e51 Menviel, L., Timmermann, A., Timm, O. E. \u0026amp; Mouchet, A. Deconstructing the Last Glacial termination: the role of millennial and orbital-scale forcings. Quaternary Sci Rev \u003cstrong\u003e30\u003c/strong\u003e, 1155-1172, doi:10.1016/j.quascirev.2011.02.005 (2011).\u003c/p\u003e\n\u003cp\u003e52 Wittmeier, H. E. et al. Late Glacial mountain glacier culmination in Arctic Norway prior to the Younger Dryas. Quaternary Sci Rev \u003cstrong\u003e245\u003c/strong\u003e, doi:10.1016/j.quascirev.2020.106461 (2020).\u003c/p\u003e\n\u003cp\u003e53 Briner, J. P., Svendsen, J. I., Mangerud, J., Lohne, O. S. \u0026amp; Young, N. E. A Be-10 chronology of south-western Scandinavian Ice Sheet history during the Lateglacial period. J Quaternary Sci \u003cstrong\u003e29\u003c/strong\u003e, 370-380, doi:10.1002/jqs.2710 (2014).\u003c/p\u003e\n\u003cp\u003e54 Glasser, N. F. et al. Cosmogenic nuclide exposure ages for moraines in the Lago San Martin Valley, Argentina. Quaternary Res \u003cstrong\u003e75\u003c/strong\u003e, 636-646, doi:10.1016/j.yqres.2010.11.005 (2011).\u003c/p\u003e\n\u003cp\u003e55 Garcia, J. L. et al. Glacier expansion in southern Patagonia throughout the Antarctic cold reversal. Geology \u003cstrong\u003e40\u003c/strong\u003e, 859-862, doi:10.1130/G33164.1 (2012).\u003c/p\u003e\n\u003cp\u003e56 Moreno, P. I. et al. Renewed glacial activity during the Antarctic cold reversal and persistence of cold conditions until 11.5 ka in southwestern Patagonia. Geology \u003cstrong\u003e37\u003c/strong\u003e, 375-378, doi:10.1130/G25399a.1 (2009).\u003c/p\u003e\n\u003cp\u003e57 Sagredo, E. A. et al. Trans-pacific glacial response to the Antarctic Cold Reversal in the southern mid-latitudes. Quaternary Sci Rev \u003cstrong\u003e188\u003c/strong\u003e, 160-166, doi:10.1016/j.quascirev.2018.01.011 (2018).\u003c/p\u003e\n\u003cp\u003e58 Davies, B. J., Thorndycraft, V. R., Fabel, D. \u0026amp; Martin, J. R. V. Asynchronous glacier dynamics during the Antarctic Cold Reversal in central Patagonia. Quaternary Sci Rev \u003cstrong\u003e200\u003c/strong\u003e, 287-312, doi:10.1016/j.quascirev.2018.09.025 (2018).\u003c/p\u003e\n\u003cp\u003e59 Putnam, A. E. et al. Glacier advance in southern middle-latitudes during the Antarctic Cold Reversal. Nat Geosci \u003cstrong\u003e3\u003c/strong\u003e, 700-704, doi:10.1038/Ngeo962 (2010).\u003c/p\u003e\n\u003cp\u003e60 Putnam, A. E. et al. Warming and glacier recession in the Rakaia valley, Southern Alps of New Zealand, during Heinrich Stadial 1. Earth Planet Sc Lett \u003cstrong\u003e382\u003c/strong\u003e, 98-110, doi:10.1016/j.epsl.2013.09.005 (2013).\u003c/p\u003e\n\u003cp\u003e61 Lee, S. Y. et al. Late Quaternary glaciation in the Nun-Kun massif, northwestern India. Boreas \u003cstrong\u003e43\u003c/strong\u003e, 67-89, doi:10.1111/bor.12022 (2014).\u003c/p\u003e\n\u003cp\u003e62 Lemieux-Dudon, B. et al. Consistent dating for Antarctic and Greenland ice cores. Quaternary Sci Rev \u003cstrong\u003e29\u003c/strong\u003e, 8-20, doi:10.1016/j.quascirev.2009.11.010 (2010).\u003c/p\u003e\n\u003cp\u003e63 Hertl, A. Untersuchungen zur sp\u0026auml;tglazialen Gletscher- und Klimageschichte der \u0026Ouml;sterreichischen Silvrettagruppe, Leopold-Franzens-Universit\u0026auml;t Innsbruck, (2001).\u003c/p\u003e\n\u003cp\u003e64 Alley, R. B. The Younger Dryas cold interval as viewed from central Greenland. Quaternary Sci Rev \u003cstrong\u003e19\u003c/strong\u003e, 213-226, doi:10.1016/S0277-3791(99)00062-1 (2000).\u003c/p\u003e\n\u003cp\u003e65 Briner, J. P. et al. Using in situ cosmogenic Be-10, C-14, and Al-26 to decipher the history of polythermal ice sheets on Baffin Island, Arctic Canada. Quat Geochronol \u003cstrong\u003e19\u003c/strong\u003e, 4-13, doi:10.1016/j.quageo.2012.11.005 (2014).\u003c/p\u003e\n\u003cp\u003e66 Buizert, C. et al. Greenland-Wide Seasonal Temperatures During the Last Deglaciation. Geophys Res Lett \u003cstrong\u003e45\u003c/strong\u003e, 1905-1914, doi:10.1002/2017gl075601 (2018).\u003c/p\u003e\n\u003cp\u003e67 Kaplan, M. R. et al. Glacier retreat in New Zealand during the Younger Dryas stadial. Nature \u003cstrong\u003e467\u003c/strong\u003e, 194-197, doi:10.1038/nature09313 (2010).\u003c/p\u003e\n\u003cp\u003e68 Cheng, H. et al. Timing and structure of the Younger Dryas event and its underlying climate dynamics. P Natl Acad Sci USA \u003cstrong\u003e117\u003c/strong\u003e, 23408-23417, doi:10.1073/pnas.2007869117 (2020).\u003c/p\u003e\n\u003cp\u003e69 Putnam, A. E. et al. Regional climate control of glaciers in New Zealand and Europe during the pre-industrial Holocene. Nat Geosci \u003cstrong\u003e5\u003c/strong\u003e, 627-630, doi:10.1038/NGEO1548 (2012).\u003c/p\u003e\n\u003cp\u003e70 Glasser, N. F., Harrison, S., Schnabel, C., Fabel, D. \u0026amp; Jansson, K. N. Younger Dryas and early Holocene age glacier advances in Patagonia. Quaternary Sci Rev \u003cstrong\u003e58\u003c/strong\u003e, 7-17, doi:10.1016/j.quascirev.2012.10.011 (2012).\u003c/p\u003e\n\u003cp\u003e71 Reynhout, S. A. et al. Holocene glacier fluctuations in Patagonia are modulated by summer insolation intensity and paced by Southern Annular Mode-like variability. Quaternary Sci Rev \u003cstrong\u003e220\u003c/strong\u003e, 178-187, doi:10.1016/j.quascirev.2019.05.029 (2019).\u003c/p\u003e\n\u003cp\u003e72 Saha, S., Owen, L. A., Orr, E. N. \u0026amp; Caffee, M. W. High-frequency Holocene glacier fluctuations in the Himalayan-Tibetan orogen. Quaternary Sci Rev \u003cstrong\u003e220\u003c/strong\u003e, 372-400, doi:10.1016/j.quascirev.2019.07.021 (2019).\u003c/p\u003e\n\u003cp\u003e73 Fischer, A., Seiser, B., Waldhuber, M. S., Mitterer, C. \u0026amp; Abermann, J. Tracing glacier changes in Austria from the Little Ice Age to the present using a lidar-based high-resolution glacier inventory in Austria. Cryosphere \u003cstrong\u003e9\u003c/strong\u003e, 753-766, doi:10.5194/tc-9-753-2015 (2015).\u003c/p\u003e\n\u003cp\u003e74 Land Tirol. (Land Tirol, Innsbruck, 2021).\u003c/p\u003e\n\u003cp\u003e75 swisstopo. (Bundesamt f\u0026uuml;r Landestopografie, Wabern, 2021).\u003c/p\u003e\n\u003cp\u003e76 Hartl, L., Felbauer, L., Schwaizer, G. \u0026amp; Fischer, A. Small-scale spatial variability in bare-ice reflectance at Jamtalferner, Austria. Cryosphere \u003cstrong\u003e14\u003c/strong\u003e, 4063-4081 (2020).\u003c/p\u003e\n\u003cp\u003e77 Fischer, A., Fickert, T., Schweizer, G., Patzelt, G. \u0026amp; Gross, G. Vegetation dynamics in Alpine glacier forelands tackled from space. Sci Rep-Uk \u003cstrong\u003e9\u003c/strong\u003e, 13918, doi:10.1038/s41598-019-50273-2 (2019).\u003c/p\u003e\n\u003cp\u003e78 WGMS. Global Glacier Change Bulletin No. 4 (2018\u0026ndash;2019). Global Glacier Change Bulletin, doi:doi:10.5904/wgms-fog-2021-05 (2021).\u003c/p\u003e\n\u003cp\u003e79 Lal, D. In situ-produced Cosmogenic Isotopes in Terrestrial Rocks. Annu Rev Earth Pl Sc \u003cstrong\u003e16\u003c/strong\u003e, 355-388, doi:10.1146/annurev.ea.16.050188.002035 (1988).\u003c/p\u003e\n\u003cp\u003e80 LDEO. Separation and Purifiation of Quartz from Whole Rock. 8 (2012).\u003c/p\u003e\n\u003cp\u003e81 LDEO. Extraction of Beryllium from Quartz. 19 (2012).\u003c/p\u003e\n\u003cp\u003e82 Nishiizumi, K. et al. Absolute calibration of Be-10 AMS standards. Nucl Instrum Meth B \u003cstrong\u003e258\u003c/strong\u003e, 403-413, doi:10.1016/j.nimb.2007.01.297 (2007).\u003c/p\u003e\n\u003cp\u003e83 Balco, G., Stone, J. O., Lifton, N. A. \u0026amp; Dunai, T. J. A complete and easily accessible means of calculating surface exposure ages or erosion rates from Be-10 and Al-26 measurements. Quat Geochronol \u003cstrong\u003e3\u003c/strong\u003e, 174-195, doi:10.1016/j.quageo.2007.12.001 (2008).\u003c/p\u003e\n\u003cp\u003e84 Claude, A. et al. The Chironico landslide (Valle Leventina, southern Swiss Alps): age and evolution. Swiss J Geosci \u003cstrong\u003e107\u003c/strong\u003e, 273-291, doi:10.1007/s00015-014-0170-z (2014).\u003c/p\u003e\n\u003cp\u003e85 Stone, J. O. Air pressure and cosmogenic isotope production. J Geophys Res-Sol Ea \u003cstrong\u003e105\u003c/strong\u003e, 23753-23759, doi:10.1029/2000jb900181 (2000).\u003c/p\u003e\n\u003cp\u003e86 Linsbauer, A. et al. The New Swiss Glacier Inventory SGI2016: From a Topographical to a Glaciological Dataset. Frontiers in Earth Science \u003cstrong\u003e9\u003c/strong\u003e, doi:10.3389/feart.2021.704189 (2021).\u003c/p\u003e\n\u003cp\u003e87 Moran, A. P., Kerschner, H. \u0026amp; Ivy-Ochs, S. Redating the moraines in the Kromer Valley (Silvretta Mountains) - New evidence for an early Holocene glacier advance. Holocene \u003cstrong\u003e26\u003c/strong\u003e, 655-664, doi:10.1177/0959683615612571 (2016).\u003c/p\u003e\n\u003cp\u003e88 Auer, I. et al. HISTALP - historical instrumental climatological surface time series of the Greater Alpine Region. Int J Climatol \u003cstrong\u003e27\u003c/strong\u003e, 17-46, doi:10.1002/joc.1377 (2007).\u003c/p\u003e\n\u003cp\u003e89 BMLRT. Vol. 2009-2018 (BMLRT, Vienna, 2021).\u003c/p\u003e\n\u003cp\u003e90 MacFarling Meure, C. et al. Law Dome CO2, CH4 and N2O ice core records extended to 2000 years BP. Geophys Res Lett \u003cstrong\u003e33\u003c/strong\u003e, L14810, doi:10.1029/2006GL026152 (2006).\u003c/p\u003e\n\u003cp\u003e91 NOAA Global Monitoring Laboratory. (NOAA Research, 2021).\u003c/p\u003e\n\u003cp\u003e92 Berger, A. \u0026amp; Loutre, M. F. in Supplement to: Berger, A; Loutre, M-F (1991): Insolation values for the climate of the last 10 million of years. Quaternary Science Reviews, 10(4), 297-317, \u003ca href=\"https://doi.org/10.1016/0277-3791(91)90033-Q\"\u003ehttps://doi.org/10.1016/0277-3791(91)90033-Q\u003c/a\u003e (PANGAEA, 1999).\u003c/p\u003e"}],"fulltextSource":"","fullText":"","funders":[],"hasAdminPriorityOnWorkflow":false,"hasManuscriptDocX":true,"hasOptedInToPreprint":true,"hasPassedJournalQc":"","hasAnyPriority":false,"hideJournal":false,"highlight":"","institution":"","isAcceptedByJournal":true,"isAuthorSuppliedPdf":false,"isDeskRejected":"","isHiddenFromSearch":false,"isInQc":false,"isInWorkflow":false,"isPdf":false,"isPdfUpToDate":true,"isWithdrawnOrRetracted":false,"journal":{"display":true,"email":"[email protected]","identity":"scientific-reports","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"scirep","sideBox":"Learn more about [Scientific Reports](http://www.nature.com/srep/)","snPcode":"","submissionUrl":"","title":"Scientific Reports","twitterHandle":"","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"stoa","reportingPortfolio":"Scientific Reports","inReviewEnabled":true,"inReviewRevisionsEnabled":true},"keywords":"","lastPublishedDoi":"10.21203/rs.3.rs-1321188/v1","lastPublishedDoiUrl":"https://doi.org/10.21203/rs.3.rs-1321188/v1","license":{"name":"CC BY 4.0","url":"https://creativecommons.org/licenses/by/4.0/"},"manuscriptAbstract":"\u003cp\u003eClimate is currently warming due to anthropogenic impact on the Earth\u0026rsquo;s atmosphere. To better understand the processes and feedbacks within the climate system that underlie this accelerating warming trend, it is useful to examine past periods of abrupt climate change that were driven by natural forcings. Glaciers provide an excellent natural laboratory for reconstructing the climate of the past as they respond sensitively to climate oscillations. Therefore, we study glacier systems and their behavior during the transition from colder to warmer climate episodes, focusing on the period between 15 and 10 ka.\u003c/p\u003e \u003cp\u003eUsing a combination of geomorphological mapping and beryllium-10 surface exposure dating, we reconstruct ice extents in two glaciated valleys of the Silvretta Massif in the Austrian Alps and find that the general ice retreat during the deglaciation after the Last Glacial Maximum (LGM) was interrupted by glacier stabilization during the Oldest Dryas to B\u0026oslash;lling transition (moraine age: 14.4 \u0026plusmn; 1.0 ka), during the Younger Dryas (YD; 12.9-11.7 ka), and during the Early Holocene (EH; 12\u0026ndash;10 ka). The first moraine age group indicates a lateral stable ice margin that postdates the \u0026lsquo;Gschnitz\u0026rsquo; stadial (ca. 17\u0026ndash;16 ka) and predates the YD. It shows that local inner-alpine glaciers were larger than during the subsequent YD until the onset of the B\u0026oslash;lling warm phase (ca. 14.6 ka), or possibly even into the B\u0026oslash;lling. The second age group ca. 80 m below the (pre-)B\u0026oslash;lling moraine indicates ice extents during the YD cold phase and captures the spatial and temporal fine structure of glacier retreat during this period. The ice surface lowered by 50\u0026ndash;60 m through the YD, which is indicative of milder climate conditions at the end of the YD compared to its beginning. Finally, the third age group falls into a period of more substantial warming, the YD\u0026ndash;EH transition, and shows discontinuous warming during the glacial to interglacial transition.\u003c/p\u003e \u003cp\u003eThe new geochronologies synthesized with pre-existing moraine records from the Silvretta Massif evidence three cold phases that punctuated the general post-LGM warming trend, and illustrate the sensitive response of Silvretta glaciers to abrupt climate oscillations in the past.\u003c/p\u003e","manuscriptTitle":"Moraines in the Austrian Alps Record Repeated Phases of Glacier Stabilization through the Late Glacial and the Early Holocene","msid":"","msnumber":"","nonDraftVersions":[{"code":1,"date":"2022-02-17 15:14:49","doi":"10.21203/rs.3.rs-1321188/v1","editorialEvents":[{"type":"communityComments","content":0},{"type":"decision","content":"Major revision","date":"2022-03-15T17:19:56+00:00","index":"","fulltext":""},{"type":"editorInvitedReview","content":"","date":"2022-03-10T08:59:07+00:00","index":"hide","fulltext":""},{"type":"reviewerAgreed","content":"e1e8bb45-df38-4436-8113-fc1c87274538","date":"2022-03-01T18:21:57+00:00","index":"hide","fulltext":""},{"type":"reviewersInvited","content":"","date":"2022-02-23T13:04:43+00:00","index":"","fulltext":""},{"type":"editorAssigned","content":"","date":"2022-02-23T12:32:13+00:00","index":"","fulltext":""},{"type":"editorInvited","content":"","date":"2022-02-14T13:15:48+00:00","index":"","fulltext":""},{"type":"checksComplete","content":"","date":"2022-02-14T13:07:59+00:00","index":"","fulltext":""},{"type":"submitted","content":"Scientific Reports","date":"2022-02-02T14:25:01+00:00","index":"","fulltext":""}],"status":"published","journal":{"display":true,"email":"[email protected]","identity":"scientific-reports","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"scirep","sideBox":"Learn more about [Scientific Reports](http://www.nature.com/srep/)","snPcode":"","submissionUrl":"","title":"Scientific Reports","twitterHandle":"","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"stoa","reportingPortfolio":"Scientific Reports","inReviewEnabled":true,"inReviewRevisionsEnabled":true}}],"origin":"","ownerIdentity":"6275cf28-54c1-45a3-b17b-bd80553c4aaa","owner":[],"postedDate":"February 17th, 2022","published":true,"recentEditorialEvents":[],"rejectedJournal":[],"revision":"","amendment":"","status":"published-in-journal","subjectAreas":[],"tags":[],"updatedAt":"2022-08-09T19:42:18+00:00","versionOfRecord":{"articleIdentity":"rs-1321188","link":"https://doi.org/10.1038/s41598-022-12477-x","journal":{"identity":"scientific-reports","isVorOnly":false,"title":"Scientific Reports"},"publishedOn":"2022-06-13 00:00:00","publishedOnDateReadable":"June 13th, 2022"},"versionCreatedAt":"2022-02-17 15:14:49","video":"","vorDoi":"10.1038/s41598-022-12477-x","vorDoiUrl":"https://doi.org/10.1038/s41598-022-12477-x","workflowStages":[]},"version":"v1","identity":"rs-1321188","journalConfig":"researchsquare"},"__N_SSP":true},"page":"/article/[identity]/[[...version]]","query":{"redirect":"/article/rs-1321188","identity":"rs-1321188","version":["v1"]},"buildId":"FbvkV6FR0MCFSLy54lSbu","isFallback":false,"isExperimentalCompile":false,"dynamicIds":[84888],"gssp":true,"scriptLoader":[]}