مدلسازی دیرینه هیدرولوژی براساس مقایسه¬ی اسناد δO^18 carbonate وδC^13 carbonate دریاچه پریشان (استان فارس) داریوش نورالهی ، دکتر حسن لشکری ، ماریا امیرزاده

نوع مقاله: مقاله پژوهشی

10.22111/gdij.2013.125

چکیده

چکیده
جهت مطالعه­ی دیرینه­ی هیدرولوژی دریاچه پریشان از رسوبات کف دریاچه مغزه­هایی به طول تقریبی m2 برداشت شد. بر روی پوسته‌ی میکروفسیل­های جدا شده از نمونه­های این مغزه­ها آنالیز ایزوتوپ کربن و اکسیژن صورت گرفت. در اینجا از نتایج این آنالیز­ها جهت مدلسازی و بازسازی شرایط هیدرولوژیکی دریاچه پریشان در طیّ 1800 سال اخیر استفاده می­شود. بر اساس تغییرات مشاهده شده در مقادیر  و   در طیّ این دوره سه زون ایزوتوپی مشخص گردید. در زون اول پایین بودن  به علت بیشتر بودن تغذیه آب­های زیرزمینی و پایین بودن  در نتیجه شرایط اقلیمی مرطوبتر تفسیر شده است همچنین همبستگی پایین  و  (14/0R2=) حاکی از شرایط هیدرولوژیکی فعالتر دریاچه بوده است. به این صورت بالانس هیدرولوژیکی مثبت­تر و به دنبال آن سطح دریاچه نسبت به امروز بالاتر بوده و معادله­ی هیدرولوژیکی دریاچه در این دوره به شکل E=P+G ارائه شده است. در زون دوم افزایش مقادیر در نتیجه­ی کاهش تخلیه آب­های زیرزمینی تفسیر شده است همچنین شواهد موجود در  نشان می­دهد که این دوره نسبت به دوره­ی قبل تا حدودی شرایط خشک­تری را تجربه کرده است. افزایش همبستگی بین  و  (2/0(R2= در این زون بسته بودن بشتر شرایط هیدرولوژیکی دریاچه است. به این صورت به نظر می­رسد که دریاچه در این دوره سطح پایین­تری را تجربه کرده باشد و بالانس هیدرولوژیکی نسبت به دوره­ی قبل  منفی­تر بوده است با این حال در این دوره نیز معادله­ی هیدرولوژیکی دریاچه از رابطه E=P+G تبعیت کرده است. بیشترین تغییرات مشاهده شده در مقادیر ایزوتوپی متعلق به این زون سوم است. افزایش ناگهانی و شدید مقادیر  به بالای صفر به علت کاهش شدید تخلیه آب­های زیرزمینی در این دوره به دریاچه تفسیر شده است. این کاهش ورودی آب­های زیرزمینی و نیز افزایش همبستگی  و  (95/0R2=) حاکی از شرایط هیدرولوژیکی نزدیک به بسته کامل است. افزایش همبستگی بین مقادیر ایزوتوپی­کربن و اکسیژن حاکی از یک سیستم عملگرای مشترک بر روی این مقادیر در این زون است. به احتمال زیاد قطع شدن نسبی ارتباط دریاچه با منابع زیرزمینی این اجازه را داده است که در طیّ فرایند تبخیر  دریاچه در موازنه با CO2جو مقادیر بالاتری را تجربه کند. به این صورت رابطه هیدرولوژیکی ارائه شده برای این زون به شکل  E=Pاست. نکته­ی مهم این است که در این زون تغییرات هیدرولوژیکی دریاچه در هماهنگی با تغییرات اقلیمی در منطقه رخ نداده است به نظر می­رسد که عامل اصلی کاهش      آب­های زیرزمینی در این زون به علت افزایش استحصال آب از طریق چاه یا قنات باشد.

کلیدواژه‌ها


عنوان مقاله [English]

Ancient Modeling of Hydrology Based on Comparison of δo18 Carbonate and the δo13 Crbonate Parishan Lake (Fars Province) Dariush Noorollahi M.Sc Climatology University of Shahid Beheshti Dr. Hassan Lashkari Associate Profesor of Natural Geography University of Shahid Beheshti Maria Amirzade Faculty of Earth science University of Shahid Beheshti

چکیده [English]

Geography and Development
10nd Year - No. 29 - Winter 2013
Received : 31/1/2012   Accepted : 17/7/2012
PP: 28 - 31
 
Ancient Modeling of Hydrology Based on Comparison of
δo18 Carbonate and the δo13 Crbonate Parishan Lake (Fars Province)
 





Dariush Noorollahi
M.Sc Climatology
University of Shahid Beheshti


Dr. Hassan Lashkari
Associate Profesor of Natural Geography
University of Shahid Beheshti




Maria Amirzade
Faculty of Earth science
University of Shahid Beheshti


 





 
Introduction
stable isotopes are strong tools for environmental studies, because most of  the elements are naturally   more abundant at least in one  isotope. Among the studies, many researchers have considered the Carbon (C13/C12), Oxygen, (O18/O16) Hydrogen (H2/H) and Nitrogen (N29/N28) which remain effects on the organic (plants and animals) and inorganic (water, soils, rocks, fossils,…) material (Griffiths, 1998, p47). In order to study the Carbon and Oxygen stable isotopes of the lake carbonates, recognizing the effective factors on the isotope's value and identifying the relationship between the isotope values is essential. In the lake environments many factors can determine the variability of the Oxygen isotopes of the lake sediments which the most important of them are including: source of materials, water temperature, residence time and the input and output amount of the lake (Benson et al, 1996, p747). In the open hydrological systems, the Oxygen isotope components of the lake water dominantly reflect the isotopic components of precipitation (rain and snow) (Leng& Marshal, 2004, p817). In addition to the effective factors on  the isotopic amount of carbon and oxygen, the relationship between the carbon and Oxygen isotopes in lake systems can deliver valuable information about the history of the lake's hydrology. The relationship between the isotope values of carbon and oxygen isotopes in the closed lakes can be based on the hydrological changes, evaporation, biomass production and the Co2 concentration (Le and Ku, 1997, p72).  There are big hydrological closed lakes especially in the arid regions, which both carbon and oxygen isotopic values are positively high. In these cases, it shows a close value of correlation .the magnitude of the correlations can be used to estimate the closeness of the lakes in different time periods. In the closed lakes, the covariance of carbon and oxygen isotope values generally indicate the interaction of carbon and oxygen isotopes with the atmosphere (Tanner, 2009, p210). In fact, the strong correlation between the carbon and oxygen isotope values indicates a common effective mechanism on the lake dissolved inorganic carbon (DIC) (Eastwood et al, 2007, p239). In the open lakes, there is a prefencally weak correlation between the carbon and oxygen isotope values. In fact, generally, the the strong correlation between the carbon and oxyegen isotope values ocuurs in the lake that have a long residence time. The correlation values more than 0.7 indicate the lake carbonates deposited in a hydrological closed lake. Furthermore, in these cases, due to the high variability of the lake water, the oxygen isotope values in the closed lake are approximately around 0.0 %. Therefore, this covariance could be used to estimate the closeness of the lakes with the carbonates deposition (Talbot, 1990, p273). Based on the methods mentioned above, a core was taken from  Parishan lake in Fars. The aim of this research is to reconstruct the hydrological condition of the lake in the past using the Carbon and Oxygen stable isotopes of the Ostracoda microfossil.





 
Ancient Modeling of Hydrology Based on Comparison of …
 
 
 
 





 
 
 
Method and Materials
The carbon and oxygen isotope components were measured in Otava university, the Faculty of Science (Earth Sciences) (G.G. Hatch Isotope Laboratories, 130 Louis Pasteur). Totally, 36 analyses of carbon and oxygen isotope were made on 33 samples. The accuracy of measurement analyses has been reported ± 0.1 per thousand.  The isotope components of samples based on the well- known scale of δ have been defined and reported as per thousand.
 
δsample (‰) = [(Rsample - Rstandard) /(Rstandard)]×1000
Where R refers to the accumulative ratios of the O18/O17 and C13/C12 in the samples and shows the isotopic standard reference. In this research both of the carbon and oxygen stable isotopes are reported based on the vpdb standards. Also the below equation is suggested in order to convert this standard into the vsmow standard.
 
VPDB-VSMOW  d18Ovsmow = 1.0309d18Ovpdb + 30.92
VSMOW-VPDB  d18Ovpdb = 0.97001d18Ovsmow -29.99
 
Discussion
According to the variation of the isotope values of the carbon and oxygen elements, three below zones were defined in order to survey the environmental changes separately.
Zone 1: (900 to 1800 BP)
When water evaporates from surface of Parishan lake, watervapor is enriched by H and 16O, because H216O has a higher watervapor in comparing with HDO and H218O (Hoefs ,2004). So the increase of evaporation enriches the lake water and consequently the carbonate of H218O.
The   values are relatively low in this zone. This indicates that evaporation had not a significant effect on the H216Olake water. As a result, Parishan Lake experienced a wet condition during this time. Furthermore, the weak correlation between the carbon and oxygen stable isotope values indicates that the lake was hydrologically open and was fed by the underground water during this zone. The existence of gypsum crystal only in this zone can show a higher fed of under ground water in to the lake. Consequently, the P+G=E is the suggested hydrological equation for this zone.
Zone 2: (200 to 900 BP)
The carbon isotopes values in this zone are relatively higher than the previous zone. Increasing the carbon isotope values could be a result of decreasing the underground water discharge into the lake. The higher O18 suggests a drier climatic condition. In fact, the higher O18 during this zone caused by removing the O17 by evaporation. The weak correlation between the carbon and oxygen isotope values suggests an open condition of Parishan Lake in this zone.  Consequently, the lake level was relatively high in this zone. However, the higher oxygen isotope values and the weaker correlation indicates that the lake level was lower than the previous period. 
 Zone 3: (Two recent centuries)
There is an abrupt and significant change in the C13 values in this zone. The carbon isotopes values exceeds 0 in this zone. The strongest correlation between the carbon and oxygen isotope values is observed in this zone. Totally, the isotopic analysis in this zone shows that 1: the increase  of carbon isotopes indicates the decrease of underground water discharge considerably in this zone. 2: the strong correlation of carbon and oxygen isotope values suggests that the lake experienced a closed condition in this zone, evaporation is a common effective factor which controls the variations of both carbon and oxygen isotope values. 3: the anthropogenic effect is an additional factor that controls the significant change of the lake hydrology. 4: the P=E equation is suggested for this zone and the current hydrological condition also indicates that evaporation and precipitation are the main effective factors on the lake hydrology.
 
Conclusion
The gradual increasing of the O18 values indicates a weak dry trend during the study period. Also the investigation of the isotope carbon show that the underground water recharges variation controlled the carbon stable isotope values. The carbon isotope changes are caused by the underground water discharge variation during different time periods. The results show that the hydrological equation of the Parishan Lake has changed during the time period as this lake experienced an open condition in the past. However, at the present, as a result of the human impact, the lakes become a closed lake where the evaporation and precipitation are the main effective factor that controls the hydrology of the lake. In the final part of the study term (zone 3) the abrupt change of the O18 suggests the impacts of the human on the lake's environment.  
 
Keywords: Palaeohydrology, Stable carbon and oxygen isotopes, Parishan Lake.
 
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