Stable isotope paleoaltimetry has provided unprecedented insights into the topographic histories of many of the world’s highest mountain ranges. However, on the Tibetan Plateau(TP), stable isotopes from paleosols generally yield much higher paleoaltitudes than those based on fossils. It is therefore essential when attempting to interpret accurately this region’s paleoaltitudes that the empirical calibrations of local stable isotopes and the relations between them are established. Additionally,it is vital that careful estimations be made when estimate how different isotopes sourced from different areas may have been influenced by different controls. We present here 29 hydrogen isotopic values for leaf wax-derived n-alkanes(i.e., δD_(wax) values,and abundance-weighted average δD values of C_(29) and C_(31)) in surface soils, as well as the δD values of soil water(δD_(sw)) samples(totaling 22) from Mount Longmen(LM), on the eastern TP(altitude ~0.8–4.0 km above sea level(asl), a region climatically affected by the East Asian Monsoon(EAM). We compared our results with published data from Mount Gongga(GG). In addition,47 river water samples, 55 spring water samples, and the daily and monthly summer precipitation records(from May to October,2015) from two precipitation observation stations were collected along the GG transect for δD analysis. LM soil δD_(wax) values showed regional differences and responded strongly to altitude, varying from.160‰ to.219‰, with an altitudinal lapse rate(ALR) of.18‰ km~(-1)(R~2=0.83; p<0.0001; n=29). These δD_(wax) values appeared more enriched than those from the GG transect by ~40‰. We found that both the climate and moisture sources led to the differences observed in soil δD_(wax) values between the LM and GG transects. We found that, as a general rule, ε_(wax/rw), ε_(wax/p) and εwax/sw values(i.e., the isotopic fractionation of δD_(wax) corresponding to δD_(rw), δD_p and δD_(sw)) increased with increasing altitude along both the LM and GG transects(up to 34‰ and 50‰, respectively). Basing its research on a comparative study of δD_(wax), δD_p, δD_(rw)(δD_(springw)) and δD_(sw), this paper discusses the effects of moisture recycling, glacier-fed meltwater, relative humidity(RH), evapotranspiration(ET), vegetation cover, latitude,topography and/or other factors on ε_(wax/p) values. Clearly, if ε_(wax-p) values at higher altitudes are calculated using smaller ε_(wax-p) values from lower altitudes, the calculated paleowaterδD_p values are going to be more depleted than the actual δD values, and any paleoaltitude would therefore be overestimated. Stable isotope paleoaltimetry has provided unprecedented insights into the topographic histories of many of the world’s highest mountain ranges. However, on the Tibetan Plateau (TP), stable isotopes from paleosols generally yield much higher paleoaltitudes than those based on fossils. It is therefore essential attempting to interpret precisely this region’s paleoaltitudes that the empirical calibrations of local stable isotopes and the relations between them are established. Additionally, it is vital that little estimations be made when estimate how different isotopes sourced from different areas may have been influenced by different controls. We present here 29 hydrogen isotopic values ​​for leaf wax-derived n-alkanes (ie, δD wax values, and abundance-weighted average δD values ​​of C_ (29) and C_ (31)) in surface soils, as well as the δD values ​​of soil water (δD_ (sw)) samples (totaling 22) from Mount Longmen (LM), on the eastern TP (altitude ~ 0.8-4.0 km above sea level (asl), a reg ion compared with the East Asian Monsoon (EAM). We compared our results with published data from Mount Gongga (GG). In addition, 47 river water samples, 55 spring water samples, and the daily and monthly summer precipitation records (from May to October, 2015) from two precipitation observation stations were collected along the GG transect for δD analysis. LM soil δD_ (wax) values ​​showed regional differences and were strongly to altitude, varying from 160 ‰ to 2.19 ‰, with an altitudinal lapse (ALR) of 18 ‰ km -1 (R ~ 2 = 0.83; p <0.0001; n = 29). These δD_ (wax) values ​​have been more enriched than those from the GG transect by ~ 40%. We found that both the climate and moisture sources led to the differences observed in soil δD_ (wax) values ​​between the LM and GG transects. We found that, as a general rule, ε_ (wax / rw), ε_ (wax / p) and εwax / sw values ​​(ie, the isotopic fraction of δD-wax corresponding to δD_ (rw), δD_p and δD_ (sw)) increased with increasing altit ude along both the LM andBasing its research on a comparative study of δD_ (wax), δD_p, δD_ (rw) (δD_ (springw)) and δD_ (sw), this paper discusses the effects of GG transects (up to 34 ‰ and 50 ‰, respectively) evapotranspiration (ET), vegetation cover, latitude, topography and / or other factors on ε_ (wax / p) values. Clearly, if ε_ (wax-p) values at higher altitudes are calculated using smaller ε_ (wax-p) values ​​from lower altitudes, the calculated paleowater δD_p values ​​are going to be more depleted than the actual δD values, and any paleoaltitude would therefore be overestimated.