Pollen-based Quaternary palaeoclimatic studies in India: an overview of recent advances

Kar, Ratan; Quamar, Md. Firoze

doi:10.1080/01916122.2017.1410502

Cited by 28 publications

(16 citation statements)

References 49 publications

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“…These are archived in loess/paleosol sediments, freshwater lake and paleolake sediments, cave deposits, and tree ring cores (for last few hundred years) among others. For example, investigations on the late Quaternary and Holocene paleoclimate shifts from NW Himalaya and Kashmir basin are commonly based on a number of multiproxy parameters including palynology (Kar and Quamar, 2018;Srivastava et al, 2017), environmental mineral magnetic studies (Basavaiah et al, 2010), dendrochronology (Borgaonkar et al, 1996;Ram and Borgaonkar, 2014), stable isotope analyses (Krishnamurthy et al, 1982(Krishnamurthy et al, , 1986Kusumgar, 1992;Kusumgar et al, 1980Kusumgar et al, , 1986, and geochemistry of sediments (Ahmad and Chandra, 2013;Babeesh et al, 2017;Chandra et al, 2016;Mishra et al, 2015), geomorphic surface processes (Babeesh et al, 2017b;Lone et al, 2017Lone et al, , 2018aLone et al, , 2018bLone et al, , 2018cShah et al, 2017), and geochronology (Meenakshi et al, 2018). As such, investigation of pedogenic paleosols and pollen profiles from Kashmir Valley have reflected warmer humid conditions and alternations of cool temperatewarm temperate-cool temperate cycles, respectively, during the past 17,000 yr BP (Agrawal et al, 1989).…”

Section: Introductionmentioning

confidence: 99%

Paleoenvironmental shifts spanning the last ~6000 years and recent anthropogenic controls inferred from a high-altitude temperate lake: Anchar Lake, NW Himalaya

et al. 2019

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Integrating multiproxy results (geochemistry, mineral magnetism, grain size, and C/N ratio variability supported by 14C AMS dating), obtained from a 1.4-m sediment core retrieved from high-altitude Anchar Lake, Kashmir Valley, NW Himalaya, we present a 6000-years record of paleoenvironmental and paleolimnological shifts. Phase 1 (6000–4700 cal. yr BP) revealed a wetter climate with a significant terrestrial input corresponding to the gradual strengthening of the westerlies. Phase 2 (4700–3900 cal. yr BP) reflects an overall improved westerly precipitation and autochthonous sources of organic matter (OM). Magnetic parameters also indicate higher lake levels and reducing conditions during this phase. Phase 2 was followed by a gradual diminishing pattern of the westerlies as also represented by phase 3 (3900–2500 cal. yr BP) and phase 4 (2500–1600 cal. yr BP) indicating moderate precipitation conditions, catchment stability, and temperate and/or cold-dry climatic conditions. Phase 5 (1600–500 cal. yr BP) revealed the prevalence of moderately cold/dry and further subdued westerly precipitation. Phase 6 (500 cal. yr BP to present) is represented by reduced westerly precipitation, shrinking lake margins, and significant terrestrial/anthropogenic controls over the lake basin. Mineral magnetic parameters indicate reducing lake bottom water conditions and eutrophication during this phase due to anthropogenic activities. These paleoenvironmental shifts reveal near synchronous changes (within dating uncertainties) with other regional paleoclimate records close to the present Anchar Lake location and reflect the gradual late-Holocene diminishment of the amount of winter/early summer moisture provided by the mid-latitude westerlies.

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Section: Introductionmentioning

confidence: 99%

Paleoenvironmental shifts spanning the last ~6000 years and recent anthropogenic controls inferred from a high-altitude temperate lake: Anchar Lake, NW Himalaya

et al. 2019

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“…Pollen grains recovered from the wetland ecosystems, which comprise lakes, reservoirs and so on, serve as an important proxy for palaeovegetation and palaeoclimate reconstructions (Chen et al, 2006; Faegri and Iversen, 1964; Gasse et al, 1991; Sun and Wu, 1987). Variations in monsoon (ISM) precipitation, its frequency and magnitude could be reflected by pollen-derived vegetation records from the wetland ecosystems (Bonnefille et al, 1999; Gaussen et al, 1965; Ghosh et al, 2015; Gunnell, 1997; Kar et al, 2002; Kar and Quamar, 2018; Prasad et al, 2014; Quamar, in preparation; Quamar et al, 2017; Rawat et al, 2015 and references therein). A considerable body of research has been carried out on palaeovegetation and palaeoclimatic reconstruction from the temperate areas of the Kashmir valley, based on megafloral remains (Puri, 1947, 1948; Vishnu-Mittre and Robert, 1973) as well as on lacustrine sedimentary pollen records (Dodia, 1988; Gupta, 1991; Gupta et al, 1984, 1988; Gupta and Sharma, 1989; Sharma et al, 1985; Sharma and Vishnu-Mittre, 1969; Singh, 1964; Vishnu-Mittre and Sharma, 1966).…”

Section: Introductionmentioning

confidence: 99%

Vegetation dynamics in response to climate change from the wetlands of Western Himalaya, India: Holocene Indian summer monsoon variability

Quamar¹

2018

The Holocene

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India’s agricultural output, economy and societal well-being are strappingly dependent on the stability of the southwest summer monsoon precipitation, its variability and extremes. Deviations in the Indian summer monsoon (ISM) precipitation may profoundly impact the agricultural productivity and gross domestic product (GDP) of the country. Understanding the spatiotemporal dynamics of the ISM precipitation during the Holocene is significant in many respects, particularly in terms of human development and establishment of centres of civilisations. Here, pollen records of the variability in ISM precipitation and their interpretation in terms of vegetation and climate change from two wetlands (Gharana and Nanga; Ramsar sites) of the Western Himalaya (India) is presented. The results suggest that between ~8536 and 5296 cal yr BP, mixed conifer/broad-leaved forests occurred in the Jammu region (Gharana Wetland sediment profile) under a cool and dry climate, probably indicating decreased monsoon precipitation. Subsequently, they were succeeded by mixed broad-leaved/conifer forests between ~5296 and 2776 cal yr BP under a warm and humid climate with increased monsoon precipitation, partly corresponding to the Holocene Climate Optimum (HCO). Between ~2776 and 1376 cal yr BP, with more expansion of broad-leaved forest elements in response to a warm and more humid climate the dense mixed broad-leaved/conifer forests came into existence in the region, indicating a further increase in monsoon precipitation. From ~1376 cal yr BP to present, the climate deteriorated, as manifested by the replacement of dense mixed broad-leaved/conifer forests by mixed conifer/broad-leaved forests in the region. The palaeoclimatic inferences drawn from the Nanga Wetland sediment profile of Samba District match with the Gharana Wetland sediment profile of Jammu District for the late-Holocene. This study provides insights into the vegetation dynamics, associated climate change and the ISM variability from the poorly understood wetland ecosystems of Southeast Asia during the Holocene.

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“…Climate change is most evidently reflected in the vegetation because the vegetation of any area is an integral and basic composition of the ecosystem, which is sensitive to and governed by the climatic changes. The distribution pattern of vegetation strongly depends on the climatic conditions (precipitation, temperature), soil characteristic and altitude, as well as human and natural impacts (Chen et al, 2006; Faegri and Iversen, 1964; Gasse et al, 1991; Ivanov et al, 2007; Kar and Quamar, 2019, 2020; Sun and Wu, 1987; and references cited therein). The influence of climate on vegetation is so great that each climatic zone has its own characteristic vegetation type.…”

Section: Introductionmentioning

confidence: 99%

“…Among various terrestrial palaeoclimate proxies, palynology is one of the most useful and reliable tools to reconstruct palaeovegetation and contemporary palaeoclimate (Birks and Birks, 2005; Kar and Quamar, 2019, 2020; Traverse, 1988; and references cited therein). Pollen and spores are well suited to examine the impact of rapid climate fluctuations on terrestrial ecosystems and the response of vegetation to climate change (Tinner and Lotter, 2001).…”

Section: Introductionmentioning

confidence: 99%

“…Pollen and spores are well suited to examine the impact of rapid climate fluctuations on terrestrial ecosystems and the response of vegetation to climate change (Tinner and Lotter, 2001). Some studies on palaeoclimatic reconstructions (Late Pleistocene-Holocene), based on palynology, are available from the central Indian core monsoon zone (Kar and Quamar 2019; Quamar, 2021; Quamar and Bera, 2017, 2020, 2021; Quamar and Kar, 2020a), which discussed the vegetation dynamics, and contemporary climate change, probably indicating the behavior of the ISM variability, around the study areas. The CMZ is the region where the variation of rainfall during the months of July and August well represents the intensity of the annual ISM rainfall (Rajeevan et al, 2010; Zorzi et al, 2015) (Figure 1a).…”

Section: Introductionmentioning

confidence: 99%

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Vegetation response to the Indian Summer Monsoon (ISM) variability during the Late-Holocene from the central Indian core monsoon zone

Quamar¹,

Kar²,

Thakur³

2021

The Holocene

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Pollen analysis and radiocarbon dating of a 1.4 m deep lacustrine sediment profile from Chhattisgarh State, central India, in the core monsoon zone (CMZ), has revealed the vegetation history, associated climate change and the Indian Summer Monsoon (ISM) rainfall variability during the Late-Holocene. The pollen evidence suggests that between ca. 3000 and 2600 cal year BP, tree-savannah vegetation occurred in the region having a comparatively lesser monsoon rainfall. The forest expanded and culminated into an open-mixed tropical deciduous forest between ca. 2600 and 2200 cal year BP under a warm and moderately humid climate with an increase in monsoon rainfall. Subsequently, between ca. 2200 and 2000 cal year BP, the existing open-mixed tropical deciduous forest transformed into a mixed tropical deciduous forest under a warm and humid climate with further increase in monsoon rainfall. Finally, between ca. 2000 and 1800 cal year BP, a dense mixed tropical deciduous forest occupied the landscape under a regime of a warm and relatively more humid climate with further strengthening of the ISM. The gradual warming, and the climatic amelioration with the intensification of the ISM, during the Late-Holocene (ca. 2600–1800 cal year BP; ~650 BC to AD150) corresponds to the Roman Warm Period (RWP), recorded globally between 2500 and1600 cal year BP (~550 BC to AD ~350). Human activities were present around the study area, which varied according to the ISM variations. The present study provides insights into the gradual intensification of the monsoon since the last ca. 2600 cal year BP (between ca. 2600 and1800 cal year BP), and an increase in the ISM strength in the CMZ of India, against the generally weakening trend during the Late-Holocene.

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Pollen-based Quaternary palaeoclimatic studies in India: an overview of recent advances

Cited by 28 publications

References 49 publications

Paleoenvironmental shifts spanning the last ~6000 years and recent anthropogenic controls inferred from a high-altitude temperate lake: Anchar Lake, NW Himalaya

Paleoenvironmental shifts spanning the last ~6000 years and recent anthropogenic controls inferred from a high-altitude temperate lake: Anchar Lake, NW Himalaya

Vegetation dynamics in response to climate change from the wetlands of Western Himalaya, India: Holocene Indian summer monsoon variability

Vegetation response to the Indian Summer Monsoon (ISM) variability during the Late-Holocene from the central Indian core monsoon zone

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