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Figure 2.3: Simulated onset and withdrawal period of the Asian monsoon as well as monsoon season length and related precipitation [mm/monsoon season], based on the definition of Wang B. and Linho, 2003. a) present-day simulation (T106_AV0k), b) difference between the present-day simulation and CMAP observations. 14 a) b)
2.3.2 Monsoon onset and withdrawal The onset and withdrawal time of the Asian summer monsoon is calculated via the simulated and observed (CMAP) relative pentad mean rainfall rates. The seasonal advance of the monsoon can only partly be represented by the model. In observations, the monsoon season first starts in the Bay of Bengal and the South China Sea. It, then, moves onto the East Asian continent and India. This typical track is depicted by the model in the Indian monsoon region, but not in the East Asian monsoon region (Figure 2.3a). Nevertheless, the monsoon season in north India starts later in the model than in observation (2-8 pentads, Figure 2.3b). In Eastern China, the simulated summer monsoon begins 2-10 pentads too early. This is partly related to the overestimated spring precipitation rate in Central Eastern China that already reaches values fulfilling the applied monsoon season criterion. The simulated monsoon retreats on most parts of the continent up to 10 pentads earlier compared to the observations. Therefore, the monsoon season length is shorter in these regions. Exceptions are the Himalaya mountain range and the area between the south- eastern Tibetan Plateau and the Bay of Bengal. The differences in simulated and observed monsoon season length are reflected in the monsoon season precipitation pattern, i.e. the precipitation falling in the monsoon season. In most parts of the continental monsoon domain, monsoon related precipitation is underestimated in the model by up to 750mm. This strongly contributes to the annual rainfall deficit in India mentioned above. 2.3.3 Near-surface air temperature The near-surface air temperature in 2m height is compared with the observational dataset of the Climate Research Unit CRU TS 2.1 (1960-2000; Mitchell and Jones, 2005) and the reanalysis data ERA40 of the European Centre for Medium-Range Weather Forecasts (ECMWF, Simmons and Gibsons, 2000). The CRU data does not include temperatures over the oceans. Temperatures are examined for two seasons. These are the wet season lasting from May to October (Figure 2.4) and the cold/dry season lasting from November to April (Figure 2.5). In both seasons, the observed/reanalysed temperature distribution is well represented in the model. The lowest near-surface temperatures are located on the elevated Tibetan Plateau and in North Eastern Asia. The highest temperatures are calculated for the equatorial regions during the cold/dry season and in the monsoon trough (i.e. North India) and the desertic regions of Africa and the Middle East during the wet season. The pattern correlation coefficient for the continental region ca. 30-170°E,10°S- 60°N of the simulated and the observed temperature is 0.99 for the cold/dry season and 0.97 for the wet season, respectively. Biases between the model and both, observational and reanalysis data, exist regarding the absolute temperature. In the wet season, simulated climate is up to 7-9K too warm in North India, East Africa and the Middle East compared 15
Page 1: Holocene climate and vegetation cha
Page 4 and 5: Anne F. Dallmeyer Max-Planck-Instit
Page 6 and 7: Overleaf Sutlej Valley, Kalpa (31°
Page 8 and 9: Zusammenfassung Mittels verschieden
Page 10 and 11: II 3.5 Summary and conclusion of Ch
Page 12 and 13: List of Figures Figure 2.1: Simulat
Page 14 and 15: Figure 4.7: Simulated differences i
Page 16 and 17: Figure A.1: The Asian monsoon regio
Page 19 and 20: 1. Introduction Like all monsoon sy
Page 21 and 22: (I) How well is the present-day Asi
Page 23 and 24: CHAPTER 5 The Tibetan Plateau exert
Page 25 and 26: 2. Simulated present-day Asian mons
Page 27 and 28: In this study, we assess the perfor
Page 29 and 30: in the local summer season. This la
Page 31: Figure 2.2: Hovmöller diagram show
Page 35 and 36: to observations and reanalysis data
Page 37 and 38: and as indices the method of prescr
Page 39 and 40: investigated by comparing atmospher
Page 41 and 42: T 3 1 _ A _ A M I P [ °C ] T 6 3 _
Page 43 and 44: - Overall, the simulation T31AV0k a
Page 45 and 46: 3. Simulated mid-Holocene Asian mon
Page 47 and 48: Values were taken from a course res
Page 49 and 50: To further analyse the differences
Page 51 and 52: Figure 3.6: Simulated difference in
Page 53 and 54: Figure 3.8: Annual cycle of precipi
Page 55 and 56: in these regions during the pre-mon
Page 57 and 58: positive anomaly (more divergent) i
Page 59 and 60: our results, we compare the reconst
Page 61 and 62: Figure 3.15: Differences in the sea
Page 63 and 64: mid-Holocene climate north of 40°N
Page 65 and 66: 4. Contribution of the atmosphere-o
Page 67 and 68: includes the dynamic vegetation mod
Page 69 and 70: Region Approximate longitude (°E)
Page 71 and 72: Figure 4.2: Seasonal and annual ave
Page 73 and 74: Figure 4.3: Same as Figure 4.2, but
Page 75 and 76: nearby desert or sparsely vegetated
Page 77 and 78: Figure 4.5: Factors contributing to
Page 79 and 80: spring summer autumn winter spring
Page 81 and 82: In autumn, the contribution of the
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Figure 4.8: Same as Figure 4.5 but
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The atmospheric response to the orb
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Due to the thermal inertia of the o
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eduction of -0.97K (on average) is
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climate in 6k. Whether the ocean-at
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econstructions (Yu et al., 2000). T
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5. Comparison of the simulated Holo
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ased vegetation reconstructions for
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(Zhang et al. 2000; Fang et al. 200
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Figure 5.2: ECHAM5 orography (eleva
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unfavourable climate conditions, i.
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vegetation type exists and the land
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etreat and were replaced by steppes
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exceeds 4000m in reality (cf. Fig.
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5.5.2 Site-specific discussion of t
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Figure 5.7: Change of the climate f
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Figure 5.8: Simulated change of sum
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Overall, the simulated forest fract
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simulated climate for SETP strongly
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6. Sensitivity of the Asian monsoon
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6.5k. Afterwards, land cover gradua
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additionally accounted for. The soi
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total grass sum per grid-box is sca
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In the dry/cold season, the strong
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6.4.1 Change of circulation and wat
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Figure 6.7: Simulated change of dif
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6.4.2 Change of albedo and turbulen
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In the dry/cold season, deforestati
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Figure 6.13: Simulated change in mo
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Northeast China (increase), regardl
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a.) Local effect: - The impact of l
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7. Summary and Conclusion 7.1 Summa
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strongest temperature change in the
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suggested in previous paleo-reconst
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Bibliography Adler, R.F., Huffman,
Page 153 and 154:
Claussen, M.: Late Quaternary veget
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Gasse, F., Arnold, M., Fontes, J.Ch
Page 157 and 158:
Joussaume, S., and Braconnot, P.: S
Page 159 and 160:
Marsland, S. J., Haak, H., Jungclau
Page 161 and 162:
Roeckner, E., Brokopf, R., Esch, M.
Page 163 and 164:
Ueno, K., Fujii, H., Yamada, H., an
Page 165 and 166:
Wu, G.X., Wang, J., Liu, X., and Li
Page 167 and 168:
Appendix A: Additional figures A.I
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Figure A.4: Sketch of the main mean
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Figure A.7: Same as Figure A.6, but
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Appendix B: Additional tables B.I S
Page 175 and 176:
Appendix C: Summary of the simulate
Page 177 and 178:
Figure C.4: Same as Figure C.1, but
Page 179 and 180:
Figure C.7: Same as Figure C.5, but
Page 181 and 182:
Acknowledgements I would like to ac
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